STATE OF UTAH DEPARTMENT OF NATURAL RESOURCES
Technical Publication No. 66
AQUIFER TESTS OF THE NAVAJO SANDSTONE NEAR CAINEVILLE, WAYNE COUNTY, UTAH
by J. W. Hood and T. W. Danielson Hydrologists, U.S. Geological Survey
Prepared by the United States Geological Survey in cooperation with The Utah Department of Natural Resources Division of Water Rights
1979
CONTENTS
Page
Conversion factors: Inch-pound to metric...... vi Abstract 1 Introduction 2 Background 2 We11- and spring-numbering system 6 Terms 6 Geologic setting 9 The Navajo Sandstone 12 Hydraulic properties of cores 13 Hydraulic conductivit Y 16 Porosity 19 Tests on discharge wells 19 Transmissivity 30 Storage coefficient 32 Long-term pumping effects 33 Chemical quality of ground water 34 Conclusions 36 References cited 37 Publications of the Utah Department of Natural Resources, Division of Water Rights 61
ILLUSTRATIONS
Figure 1. Map showing location of the lower Dirty Devil River basin area and the test area near Caineville . 3
2. Map showing geology of the test area and location of wells and springs near Caineville . 4
3. Diagram showing wel1- and spring-numbering system used in Utah . 7
4. Generalized east-west section showing folding in the Navajo Sandstone . 11
5. Photomicrographs of core sample 76UT1, Navajo Sandstone ..... 14
6. Graph showing particle-size distribution for four cores from the Navajo Sandstone . 15
7. Photomicrographs of core sample 76UT2, Navajo Sandstone ..... 16
8. Photomicrographs of core sample 76UT3, Navajo Sandstone ..... 17
9. Graph showing hydraulic conductivity and porosity of core samples from the Navajo Sandstone . 20
iii Illustrations--Continued
Page
Figure 10. Graphs showing water levels in wells in the Red Desert...... 24
11. Graphs showing relation of water level in well OW-1A to change in barometric pressure and earth tides 25
12. Graph showing water levels in well OW-1A 25
13. Representative data analyses from 35-day aquifer test ..... 26
14. Graph showing analysis of residual drawdown in well TW-l after pumping for 35 days 28
15. Graph showing analysis of residual drawdown in well TW-l after pumping for 11 days at increasing rates of discharge...... 29
16. Graph showing drawdown as a function of distance from well TW-l after pumping for 30 days 31
17. Graphs showing water levels in wells (D-28-7)36bbb-l and (D-28-8)29cdc-l 32
18. Graph showing theoretical effect of long-term pumping at well TW-l 33
TABLES
Table 1. Formations that crop out in or underlie the Caineville area . 10
2. Grain-size diameters of four cores from the Navajo Sandstone 12
3. Statistical characteristics of grain-size analyses, specific gravity, and carbonate content of four cores from the Navajo Sandstone 13
4. Hydraulic conductivity and porosity determined by the Geological Survey for core samples from wells TW-l and OW-1A 18
5. Hydraulic conductivity and porosity determined by Chemical and Geological Laboratories, Casper, Wyo., for core samples from wells TW-l and OW-1A 18
iv Tables--Continued
Page
Table 6. Hydraulic conductivity and porosity determined by Core Laboratories, Inc., Wilmington, Calif., for core samples from wells TW-1 and QW-1A 19
7. Summary of results from aquifer tests 22
8. Records of selected wells and springs 39
9. Selected logs of wells . 40
10. Selected chemical analyses of water samples . 58
11. Measurements of discharge, temperature, and specific conductance of water from wells . 59
v CONVERSION FACTORS: INCH-POUND TO METRIC
Most values in this report are given in inch-pound units followed by metric units. The conversion factors are shown to four significant figures. In the text, however, the metric equivalents are shown only to the number of significant figures consistent with the accuracy of the value in inch-pound units.
Inch-pound Metric Unit Abbreviation Unit Abbreviation (Multiply) (by) (to obtain)
Acre 0.4047 Square hectometer hm 2 .004047 Square kilometer km 2 Cubic foot per (ft 3 /d)/ft .0929 Cubic meter per (m 3 /d)/m day per foot or ft 2 /d day per meter or m2 /d Foot ft .3048 Meter m Gallon per gal/min .06309 Liter per second L/s minute Gallon per (gal/min)/ft .2070 Liter per second (L/s)/m minute per per meter foot Inch in. 25.40 Millimeter rnrn 2.540 Centimeter ern Mile 1.609 Kilometer km 2 Square foot .0929 Square meter m
Chemical concentration and water temperature are given only in metric units. Chemical concentration is given in milligrams per liter (mg/L) or micrograms per liter (Wg/L). Milligrams per liter is a unit expressing the concentration of chemical constituents in solution as weight (milligrams) of solute per unit volume (liter) of water. One thousand micrograms per liter is equivalent to one milligram per liter. For concentrations less than 7,000 mg/L, the numerical value is about the same as for concentrations in the inch-pound unit, parts per million.
Chemical concentration in terms of ionic interacting values is given in milliequivalents per liter (meq/L). Meq/L is numerically equal to the inch-pound unit, equivalents per million.
Water temperature is given in degrees Celsius (OC), which can be converted to degrees Fahrenheit (OF) by the following equation: OF = 1.8(OC) + 32.
vi AQUIFER TESTS OF THE NAVAJO SANDSTONE NEAR CAINEVILLE, WAYNE COUNTY, UTAH
by
J. W. Hood and T. W. Danielson Hydrologists, U.S. Geological Survey
ABSTRACT
Ground water in the Navajo Sandstone near Caineville, Wayne County, Utah, was studied during 1975-77 as part of an investigation of water in bedrock in the lower Dirty Devil River basin area. The purpose of the study near Caineville was to determine the water-bearing properties of the Navajo by utilizing data obtained mainly during test drilling and aquifer testing by the Intermountain Power Project.
Consolidated rocks that crop out in the area range in age from Cretaceous to Jurassic. The area is underlain by older Mesozoic and Paleozoic sedimentary rocks that extend to a depth of at least 7,160 feet (2,182 meters) . The Navajo Sandstone is the major known aquifer in the area, yield ing 2,800 and 3,110 gallons per minute (177 and 196 liters per second) to two test wells near Caineville.
The Navajo Sandstone is massive, crossbedded, very fine to fine grained, and approximately 900 ft (274 meters) thick. For the practical purpose, of aquifer analysis, it is hydraulically isotropic in unfractured parts. It has an average hydraulic conductivity of 0.5 foot per day (0.15 meter per day), and an inferred transmissivity of 450 feet squared per day (42 meters squared per day).
Folding of the sandstone has produced fracturing that probably permits some interformational leakage. The leakage under natural conditions is up ward, under high artesian head; and it probably contributes to the salinity of the water in the sandstone.
Fracturing of the sandstone has enhanced the permeability and made the formation heterogeneous and probably anisotropic on a regional scale. Values for transmissivity, obtained from tests of various lengths, range from 1,330 to 4,250 feet squared per day (124 to 395 meters squared per day). This indicates that conventional aquifer-test analysis does not yield the uniform results that might be expected of the relatively homogeneous sandstone.
For the purpose of calculating long-term pumping effects, a generalized selected value for transmissivity of the Navajo Sandstone is 1,500 feet squared per day (139 meters squared per day); and a generalized selected value for the storage coefficient under artesian conditions is 0.001. For water table conditions, the value for the specific yield is estimated to be between 5 and 10 percent.
1 INTRODUCTION
This report presents part of the results of a study of water in bedrock in the lower Dirty Devil River basin area in parts of Emery, Garfield, and Wayne Counties, Utah (fig. 1), with special emphasis On the Navajo Sandstone of Triassic and Jurassic age. The study was made by the U.S. Geological Survey in cooperation with the Utah Department of Natural Resources, Division of Water Rights. Fieldwork was carried out July 1975-September 1977.
The purpose of this report is to present the results of test drilling and aquifer testing in the Navajo Sandstone in and near the Red Desert northwest of Caineville (fig. 2) and related data acquired during the investigations carried out by the Intermountain Power Project during 1975-76. Data in the report include aquifer-test analyses, core analyses, selected records of wells and springs, and selected chemical analyses.
Caineville is near the southeast corner of T. 28 S., R. 8 E., approx imately 17 mi (27 km) west of Hanksville in Wayne County. The test area is mainly in the Red Desert, a deeply dissected erosional valley in the south central part of T. 28 S., R. 8 E.; it includes wells in secs. 29 and 33. Observations also were made at wells and springs in T. 28 S., R. 7 E., to the west.
Background
The Intermountain Power Project (IPP) is the successor to the Inter mountain Consumers Power Association (ICPA) in the planning for construction of a coal-fired electric-generation plant in the area. Preliminary studies began about 1971, and in the winter of 1973-74, ICPA drilled a test well in the NW~SW~SE~ sec. 29, T. 28 S., R. 8 E. (fig. 2). This location was recommended by S. B. Montgomery of the Utah Division of Water Resources because it was at the point of minimum depth to the Navajo Sandstone near an oil test that reportedly discharged large amounts of water during the drilling of the Navajo section.
The ICPA test well yielded 3,110 gal/min (196 L/s) during a test on February 8-9, 1974 (R. J. Madsen, ICPA, written commun., 1974). Subsequently, IPP drilled a test well (TW-1) in the northwest corner of sec. 33, T. 28 S., R. 8 E., reconditioned an oil-test well in the southern part of sec. 33 (the Colt well), and drilled an observation well (OW-1A) in sec. 27, T. 28 S., R. 7 E., 5 mi (8 km) west of TW-1. These wells, together with an existing stock well (the Stanolind well) in sec. 29, T. 28 S., R. 8 E., were used during an extensive aquifer test. (See table 8 and fig. 2.)
All construction and testing were the responsibility of IPP, under the direction of the Los Angeles Department of Water and Power, a participant in IPP. The Geological Survey provided some gaging and recording equipment, and personnel of the Geological Survey and the Utah State Engineer's office made supplementary measurements at observation wells at the beginning of pumping and recovery during the principal aquifer test. The Geological Survey also made parallel check determinations on cores and water samples taken by IPP.
IPP provided a wealth of data regarding well construction and testing, and IPP and the Geological Survey joined in compiling a composite of aquifer test records. The writers gratefully acknowledge the ready cooperation given by the officers and personnel of IPP.
2 EXPLANATION 42 0 I:!: iI!: I General study area
BOX. Test area near Cainevi 11e (area shown in fig. 2)
20 40 60 MI LES I i I " I 40 I 20 60 KILOMETERS I~ 0 III 0 110 41 0 rl------l--~H;:+_
/ I, ~ I
'> Tooele I o \ T o o E L E "',-/ I \ '> ( ( 40 0 ------~~ / '; ':"..-, \------" /L~, ) > '-\"----~ Nephi J fl AB 0/" 1- I\ , 1\ '-0 1 I\I G' J I \ 'I_ I ' _ -.J I SANF'ETE-r' 0M a n ~ i '1-
I L \., -f\ --CJ"" - -=::o_~~ :< J ::'_\_J{ ! ',- ~-- /.-J' ( '/ BEAVE /R - )I ~> _r- ! /' ------~----- I I I '~------"~----j-__;c.-:...----I--+__--_*_ 38 0 +--,-/-----i-J~~~+---+---'-\\\138 0 I #",' , "?"'Parowan~ .I Mondcell~0 R N 0 __ J' \ '1 I
( ) 0 N () ~S AN I 'v/ I
\ (/, I \ ~ ~ \ \ 37" -~,-" 37° 0 0 114 113 III 0
Figure I.-Location of the lower Dirty Devil River basin area and the test area near Caineville.
3 \c::.:_~=--- 0 ...,";::....;:;:;/;;j f'~Y;,:--=- 10 \ Ix:~d;f~~:/::::·. :\ 6]7:':'-:-:'; f====F==E=:=====E=====-~/--:--/ ~------""""$\ ",."0 --1:------~ .j:- ~~:,:~ ~I~~~~~~~~~~~~~!~~I~~ ..,.,.".,.,& 'j[n."...!- - =j)n~ -=-=-=-=-=====---====::::.:.~~--- ~- .,.,:,:,:,·,:'A - -~ ~ ~ ~ .•..• loU I le - ~ - )" :: :1\1\ ::.:-::::-:·1r··· .. · / I- .----=---=--~-~ I 1..... ::1 r C
T. 29 S.
Jc KJcb
Base after Wi I Iiams Scale:l:62,500 Geo logy f rom WI II iams and and Hackman (1971) o 1 2 MILES Hackman (1971). Hydrology J ~ by W. Hood, 1977 I I II I! I 'I I! 1 II I !! I 1 I o 1 2 3 KILOMETERS EXPLANATION
Qa Alluvium Contact > I I et "":z: 100~ UJ I Qae I Alluvium and eolian deposits Dip and strike of beds ""l et ':3 Ant icl ine 0' ~ I Qt I Terrace gravels t-- Showing di reet ion of plunge ~ t Syncline ~ Emery Sandstone Member Showing direction of plunge
CIl Flow ing we 11 k~'b Blue Gate Member •TW-l - IIIII,." IIIII TW-l is name of well used in text .c'" (I) (see table 8)
rJ) 0 FKmfg Ferron Sandstone Member o Non flow ing we 11 U c oi 1- tes t we 11 :::E'" Tununk Member \J1 E!-;;!=j + ...--..- Perennial spring Tununk Member of Mancos Shale fl~td=j and Dakota Sandstone, undivided 0---.- Intermittent spring I '- Cedar Mountain Formation and I KJcb I Brushy Basin Shale Member of Morrison Formation, undivided
[··············~I Salt Wash Sandstone Member of ::::Jms:::::...... Morrison Formation u
(I) (I) Summerville Formation and
I Jc I Carmel Formation
Figure 2.-Geo1ogy of the test area and location of wells and springs near Cainevi11e. Well- and spring-numbering system
The system of numbering wells and springs in Utah is based on the cadastral land-survey system of the U.S. Government. The number, in addition to designating the well or spring, describes its position in the land net. By the land-survey system, the State is divided into four quadrants by the Salt Lake base line and meridian, and these quadrants are designated by the uppe~9ase letters A, B, C, and D, indicating the northeast, northwest, southwest, and southeast quadrants, respectively. Numbers designating the township and range (in that order) follow the quadrant letter, and all three are enclosed in parentheses. The number after the parentheses indicates the section, and is followed by three letters indicating the quarter section, the quarter-quarter section, and the quarter-quarter-quarter section--generally 10 acres (4 hm2); 1 the letters a, b, c, and d indicate, respectively, the northeast, northwest, southwest, and southeast quarters of each subdivision. The number after the letters is the serial number of the well or spring within the 10-acre (4_hm2 ) tract; the letter "S" preceding the serial number denotes a spring. If a well or spring cannot be located within a 10-acre (4-hm2) tract, one or two location letters are used and the serial number is omitted. Thus (D-28-8)29cdc-l designates the first well constructed or visited in the SW~SE~SW~ sec. 29, T. 28 S., R. 8 E., and (D-28-7)11cdb-Sl designates a spring in the NW~SE~SW~ sec. 11, T. 28 S., R. 7 E. The numbering system is illus trated in figure 3. In the Emery-Garfield-Wayne-Counties study area, several wells have been substantially modified. This applies particularly to petroleum-test wells that have been converted to water wells; such conversion entirely alters the characteristics of the well. In this report, the serial number may be followed by a letter: W, indicates a petroleum-test well that has been converted to a water well; S, indicates a well that has been plugged back.
Terms
The following terms for aquifer characteristics that are used in this report are given precise definitions by Lohman and others (1972):
Term Abbreviation Units
Hydraulic conductivity K ft/d [( ft3I d) 1ft2 ] Porosity n dimensionless decimal fraction (or percent- age) Specific capacity Sc (gal/min)/ft Specific yield Sy dimensionless decimal fraction (or percent- age) C' Storage coefficient L) dimensionless decimal fraction ,n Transmissivity L ft2 /d [( ft3Id)1ft]
lAlthough the basic land unit, the section, is theoretically 1 mi 2 (2.6 km2), many sections are irregular. Such sections are subdivided into 10-acre (4-hm2 ) tracts, generally beginning at the southeast corner, and the surplus or shortage is taken up in the tracts along the north and west sides of the
6 Sections within a township Tracts within a section
Sec. 29
6 5 ij 2
7 8 9 II ;2 b a
18 17 16 15 13
20 21 22 2ij I b I a I 29 28 27 26 ---c-i- d • I b I a L-d - 3ij 31 32 33 35 c I d Well 6miles (9.7 ki lometers) I (1.6 ki lometers) ~ (D-28-8)29cdc-1 , I B A L_ SAL T BASE LINEI "Salt Lake City \ I I I I I ~ \ I I c D I I ~ : /- , I 1. 28 S., R. 8 E. I I _____ J Figure 3.-Well- and spring-numbering system used in Utah.
7 The relations between inch-pound units, metric units, and units of abandoned terms for K and Tare given in the following table, adapted from Lohman and others (1972, p. 18). Relation of units Equivalent values shown in same horizontal lines tindicates abandoned term A. Hydraulic conductivity t Field coefficient Hydraulic conductivity of permeability (K) (pf) Feet per day Meters per day Gallons per day (ftld) (mid) per square f~ot [(gal/d)/ft ] One 0.3048 7.48 3.2808 One 24.54 .1337 .0407 One B. Transmissivity Feet squared per Meters squared per Gallons per day ~ay day per foot (ft Id) (m 2 /d) [(ga1I d ) 1ft] One 0.092903 7.48 10.7639 One 80.514 .1337 .012421 One
Some of the permeability determinations were made by oil-industry service companies who reported their determinations in ~illidarcies (or 0.001 Darcy). The Darcy has the dimensions 0.987 x 1O-/jcm2 (at 20oC). For comparison with other results, these values were converted as follows: K(at 60 oF) = 2.439 x millidarcies 1, 000 Other abbreviations
The following additional abbreviations are used in this report: Q,discharge, in specified units, r,distance from the pumped well, S,drawdown, s',residual drawdown, t,time in specified units, u, W(u),values from the abscissa and ordinate, respectively, of the Theis non-equilibrium type curve. (See Ferris and others, 1962, p. 92-98.)
For image well analyses, the subscript r, as in s, refers values ascribed to the real, or pumped well. The subscript & refersrto values ascribed to the image well.
8 Chemical-quality terms
The terms used by the U.S. Geological Survey to classify water according to the concentration of dissolved solids, in milligrams per liter, are as follows:
Fresh Less than 1,000 Slightly saline 1,000- 3,000 Saline Moderately saline 3,000-10,000 Very saline 10,000-35,000 Briny More than 35,000
Geologic setting
Consolidated rocks that crop out in the test area near Caineville range from the Mancos Shale and its several members of Cretaceous age to the Carmel Formation of Jurassic age (fig. 2). Beneath the Carmel, the geologic section contains Mesozoic and Paleozoic sedimentary rocks that extend to a depth of at least 7,160 ft (2,182 m). (See log of well (D-28-8)29cdc-2, table 9.)
The geologic units are described by Baker (1946), Gilluly (1929), Hunt (1953), and Smith, Huff, Hinrichs, and Luedke (1963); and water in some of the units is described by Feltis (1966). The areas of outcrop and the major structural features are shown on the geologic map of Utah (Stokes, 1964), and the geologic structure is shown in greater detail by Williams and Hackman ( 1971 ). The reader is referred to these sources for descriptions of the formations and a regional perspective of the structures that distort the rocks. The formations that crop out in the area of figure 2 and immediately underlie the area are listed in table 1.
Rocks in the test area are folded. The area contains the Caineville anticline and the Saleratus Creek syncline. These two folds lie between two monoclines--the Waterpocket Fold to the west and the Caineville monocline to the east. (See fig. 2.) Where the Navajo Sandstone crops out (not shown in fig. 2) in the Waterpocket Fold (fig. 4), the rocks dip 90 to 130 ENE. Surface dips around North Blue Flat near the axis of the Saleratus Creek syncline are about 50 on both sides and dips on the sides of the Caineville anticline are 50 to 11 0 . At the Caineville monocline, the rocks have steep dips of 19 0 to 25 0 E. The Red Desert is on the apex of the Caineville anticline which plunges about 2lo N. and an unmeasured amount south.
One result of this large-scale folding is the fracturing of competent formations such as the Navajo and Wingate Sandstones. Where exposed in the Waterpocket Fold, both of these sandstones exhibit close-to~wide-spaced joints that parallel the trend of the fold (Hunt, 1953, figs. 94 and 97). It can be inferred that similar jointing or fracturing occurred to the east, with the maximum effects occuring at the bottoms of the formations in the Saleratus Creek syncline and at their tops in the Caineville anticline. Some cross fracturing probably is also present due to the plunge of those structural features. Such inferred tension features cannot be seen because the formations are buried, but even the less competent siltstone of the Entrada Sandstone in the Red Desert, the principal trend of gypsum-filled fractures is northward, parallel to the trend of the anticline.
9 Table 1.-Formations that crop out in or underlie the Caineville area
Age Formation Remarks
QUATERNARY Unconsolidated rocks Contain water only beneath stream channels. Water generally high in dis solved sol ids.
CRETACEOUS Mancos Shale: Emery Sandstone Member Caps south Caineville Mesa. Blue Gate Member Low permeability. Ferron Sandstone Member At edge of Caineville Monocline. Gen erally low permeability. Tununk Member At edge of Caineville Monocline and in bottom of North Blue Flat. Low per meability. Dakota Sandstone Generally thin, where present. Cedar Mountain Formation Conglomerate in bottom may locally be an aquifer. Generally low permeabil ity.
JURASSIC Morrison Formation: Brushy Basin Shale Member Contains variegated beds of bentonite. Generally low permeability. Salt Wash Sandstone Member Yields perched water under artesian pressure at well (D-28-7)36bbb-1. Contains gypsum. Summerville Formation Contains gypsum. Generally low per meability. Curtis Formation Caps bluffs of Entrada Sandstone. Gen erally low permeability. Entrada Sandstone Yields water to wells in adjacent areas. Overall permeability is low. Carmel Formation Yields water where fractured or includ ed limestone is cavernous. Water gen erally is saline.
JURASSIC AND TRIASSIC(?) Navajo Sandstone Major aquifer. Massive sandstone. Water saline where deeply buried.
TRIASSIC(?) Kayenta Formation Contains siltstone beds that separate Navajo and Wingate aquifers.
TRIASSIC Wingate Sandstone Potentially a source of water to supple ment that from Navajo Sandstone. Probably has lower intergranular per meability than Navajo but probably equal to it in fracture permeability. Not as thick as Navajo. (See log of well (D-28-8)29cdc-2 in table 9.) Chemical quality of water near Caine ville unknown but probably more saline than Navajo. Chinle Formation Generally low permeability. Shinarump Member Mainly sandstone in this locality. Thin and discontinuous. Moenkopi Formation Contains some sandstone. Overall per Sinbad Limestone Member meability is low.
PERMIAN Kaibab Limestone Both formations may have potential for Coconino Sandstone development of suppl ies of slightly to moderately saline water.
10 - . Q> • ~ c=
<>.E0" E c= 0 "; U _c= . c= Q> ,, (]) 0_ c E .- o +' 1Il "0
U C -Q> '" Cl C 3: o ..c: 1Il c o +'u (]) 1Il +' 1Il ~ I +' 1Il "0 (]) N '" '" '" '" "' -'" '" L-L-I I I l I I S J a I a W I _LI I 1 I I a a J '" '" '" '" '" '" '"N ...'" '" '" '" '" N "' '""' ... M '" -'" lB31 ns Nnw BOey 30nlllH 11 THE: NAVAJO SANDSTONE: The Navajo Sandstone is a massive, strongly and intricately cross bedded, gray to pale-brown sandstone, which is mostly very fine to fine grained. Grains of sand in the formation are subangular to well rounded (fig. 5). In the Red Desert area, the sandstone is about 900 ft (274 m) thick, and it thins eastward and thickens westward. The lower contact with the underlying Kayenta Formation is transitional, and the two formations probably intertongue. The upper contact with the overlying Carmel Formation is marked in most areas by a bed of red sandstone and gypsiferous siltstone. The red bed is overlain by as much as 20 ft (6 m) of a sandstone similar to the Navajo; and although the sandstone may be a part of the hydrologic system in the Navajo, it is considered to be a basal part of the Carmel. Most of the Navajo Sandstone has little of the parallel bedding common to sedimentary rocks. True bedding planes are rare and generally are 50 ft (15 m) or more apart. However, crossbedding occurs on a large scale, and the crossbedding laminae may truncate one another any any angle. Dips of these 0 laminae are as great at 30 . The formations seems to be slightly coarser and less consolidated near its top. Drilling-time logs for wells TW-1 and OW-1A indicate that penetration rates, though variable, tended to decrease with depth in the formation. This also is borne out by the drilling experience at the ICPA test well, which was terminated at 761 ft (232 m) owing to the inflow of loose sand. The discussion in the following sections is based upon well logs (including sample examination and analysis of representative cores) , laboratory determination of hydraulic properties, and discharging-well tests. Table 9 contains logs of four wells that penetrate the Navajo Sandstone. The drill cuttings described for the two test holes, however, at times were badly contaminated with caved material from zones above the sample intervals. Three representative zones in well TW-1 and one such zone in well OW-1A were cored. Tables 2 and 3 give the results of sieve analyses and related statistics for four core samples, and figure 6 summarizes the distribution of grain sizes in those samples. Figures 5, 7, and 8 show photomicrographs of thin sections of the three samples from well TW-1. Table 2.--Grain-size diameters, in millimeters, of four cores from the Navajo Sandstone, in percentage by weight. (See also fig. 6.) Sand Well Laboratory Clay Silt Very fine Fine Medium Coarse Very coarse sample No. <0.004 0.004-0.0625 0.0625-0.125 0.125-0.25 0.25-0.5 0.5-1.0 1.0-2.0 TW-1 76UT1 4.9 31.7 30.8 32.3 0.21 0 76UT2 6.5 57.6 35.2 .66 0 0 76UT3 12.6 53.5 33.4 .51 0 0 OW-1A 76UT24 6.2 0.98 41.3 45.6 5.7 .23 0 12 Table 3.--Statistical characteristics of grain-size analyses, specific gravity, and carbonate content of four cores from the Navajo Sandstone Specific gravity Well Laboratory Median size Sorting Uniformity of solids Carbonate l 2 J 4 6 sample No. (mml coefficient Skewness Ku rtosis coefficientS (gm/cel content TW-l 76UTl 0.17 1.7 1.0 0.29 3.0 2.66 0 76UT2 .11 1.4 1.1 .27 1.8 2.70 0 76UT3 .10 1.4 1.1 .2~i 2.3 2.69 0 OW-1A 76UT24 .13 1.5 .96 .30 2.3 2.68 0 ~ [Median d so ' 2Geometric quartile deviation, taken from cumulative curves representing frequency data of sediments. va-lOt'3 Q ~ 25 percent quartile, Q ~ 75 percent quartile. 3 [ J(Q x Q )/(median)2. I J 4 (OJ - Q )/2(P - P ) taken from cumulative curves. P ~ 90 percentile, P ~1 0 percentile. _[ 90 10 90 10 sUniformity coefficient sorting index ~ d /d ' 60 I0 6Calcium carbonate equivalent by carbon dioxide absorption method. The megascopic core descriptions in the logs for wells TW-1 and OW-1 A (table 9) contain the statements that the sandstone includes some calcite and gypsum, mainly as fracture or vein fillings. The bulk of the sandstone, however, has no carbonate cement. (See table 3.) In sample 76UT1, the biomodality due to the laminae of two different grain sizes is apparent in the sieve analysis stated in table 2 and depicted in figure 6. Despite the general lack of matrix or cement, the volume amount of interstices (pore spaces) is measurably reduced by the packing of the subangular to subrounded grains. Hydraulic properties of cores Core tests were made because they yield information that cannot be obtained from field tests. Laboratory values for hydraulic conductivity (x) show the primary permeability of the sandstone; whereas, field tests are strongly influenced by secondary features, such as fracturing. Porosity (r) can be determined only by laboratory methods, although the value can be closely approximated from certain borehole geophysical logs. Sample cuts from cores in wells TW-1 and OW-1A were submitted to the Hydrologic Laboratory of the Geological Survey, Denver, Colo., and to two commercial laboratories. The results are listed in tables 4, 5, and 6, and the results are compared in figure 9. The tables indicate slightly different conditions of analysis at each laboratory, and the figure shows that despite the slightly different depths of the samples, one laboratory apparently obtained generally larger values for both K and n. The values for K, as determined by the Geological Survey for the three samples from well TW-1, are lower than those from the other laboratories because the Survey adjusted the values to show K under loaded conditions at the present depth of burial. 13 • Ordinary light Magn; f Icat ion x 20 Polarrzed light (crosse,1 Nicols) Ordinary light Magni f icat ion x 40 Figure 5.-Photomicrographs of core sample 76UTI, Navajo Sandstone. 14 U.S. standard sieve number or size opening 230 125 60 35 18 99.9~ IIII II I' 1." I ,I, .;/ -----= 99.8 1'1 -::,\"/1/1,,;91.--- ,,<0," \ / " /0 -::,'\ / • 99.51 /,',,'0 // 99.01 .. // 98'- // / 95 / / / /! ! ! 90 / / .. / ! ! / ! ,I / I / / '"w ! ) Z . / !.. /"- !! / /.;:,'\ .... I~'O' z ,'! w i! // t-' '-' 40r \Jl '"w I, 0.. 30 r I 20 f- }! ! ,/II/ 10L ______liIl.l1..! ------~/// 5 2 1. 0,51 i 0, 2f- O. 11 II I I II 0.001 0.01 0.1 1.0 DIAMETER. IN MILLIMETERS Figure 6.-Particle-size distribution for four cores from the Navajo Sandstone (See also table 2.) .~ 'i • ~ .. .,. ill .",., • '. ",' • '. • • " Ordinary light Mag n i fie a t i 0 11 X 20 PolarIZed light (crossed Nicols) Figure 7.- Photomicrographs of core sample 76UT2, Navajo Sandstone, Hydraulic conductivity The average value for horizontal hydraulic conductivity for the Navajo Sandstone, using all determinations in tables 4-6, is 0.64 ftld (0.020 mid) . One value for K in table 6 is nearly twice larger than the next lowest value, and the high value may be anomalous. The average K without this high value is 0.55 ftld (0.17 mid). Eight determinations have values for both horizontal and vertical K. The averages for these eight pairs yield a ratio of horizontal to vertical K of 1.42:1. Most aquifers are stratified and therefore more strongly anisotropic. As described in several of the references on aquifer theory, anisotropy requires adjustment of aquifer-test data before reliable hydraulic coefficients of the aquifer can be determined. In contrast to the Navajo Sandstone, the lowest ratio of horizontal to vertical K for most stratified aquifers appears to be about 5: 1 j the ratio generally is larger. (For example, see Bennett and others, 1967, p. G55.) 16 Ordinary ligfll Magnl f Ical Ion x 20 PolarlZe,j l,glll (crosse,j Nicols) Ordillary light ~agrl i f I cat ion x 40 Figure B.-Photomicrographs of core sample 76UT3, Navajo Sandstone. 17 Table 4.--Hydraulic conductivity and porosity determined by the Geological Survey for core samples from wells TW·1 and OW-1 A Hydraulic conductivity at 60°F (15.5°C) measured in meters per day. using simulated formation water synthesized from chemical analyses of water from the two wells; effective porosity is for voids having entrance diameters larger than 0.1 micron. Depth below Depth below top Hydraulic conductivity Porosity Well Laboratory Iand su rface of formation Horizontal Vertical (Percent) sample No. (h) (ftl mid hid mid hid Total Effective TW-1! 76UT1 834.7 835.2 126 0.087 0.29 0.046 0.15 21.8 20.3 76UT2 1.139.7 1.140.3 431 .047 .15 .018 .059 25.3 22.3 76UT3 1,476.3 1,476.8 767 .0040 .013 .0096 .031 24.8 22.5 OW-1A 76UT24 2.350.2 2.350.5 361 .21 .69 .14 .46 22.6 20.5 ! Specimens from the three cores from this well were cut so that the horizontal K is that parallel to the bedding planes and the vertical K is that normal to the bedding. The three pairs of determinations were made in a tri-axial loading chamber under various effective stresses. The values for K given are those estimated for the estimated in situ effective vertical stress. Table 5.--Hydraulic conductivity and porosity determined by Chemical and Geological Laboratories, Casper, Wyo., for core samples from wells TW-1 and OW-1A Determinations! were from splits of the core samples analysed by the Geological Survey (table 4). Horizontal Vertical Permeability Hydraulic Permeability Hydraulic Well Laboratory (millidarcies) conductivity Porosity (millidarciesl conductivity Porsity sample No. Air Water mid hid (percent) Air Water mid hid (percent) TW-1 76UT1 626 173 0.128 0.421 21.9 263 44 0.0326 0.107 22.8 76UT2 560 166 .123 .404 22.1 498 158 .117 .384 23.4 76UT3 381 138 .102 .336 22.0 347 90 .0667 .219 22.7 OW-1A 76UT24 460 148 .110 .360 20.7 569 190 .141 .462 21.1 ! One-inch horizontal and vertical plugs were drilled and dried and permeability and porosity measurements to dry air were made. The plugs were then saturated with Casper tap water for 48 hours and flow rates to water were determined aher at least 10 pore volumes had been flushed and equilibrium had been reached. Because of its low ratio of horizontal to vertical K, the Navajo Sandstone in and near the Red Desert is, for practical purposes in analyzing aquifer tests, considered to be isotropic. The average K from laboratory tests is about 0.5 ft/d (0.15 mid). Based on the value of 0.5 fUd, the 2 t 2ansmissivity (T) of the 900-ft (274-m) section of Navajo is 450 ft /d (42 mid), where it is not enhanced by fractures or other secondary openings. 18 Table G.--Hydraulic conductivity and porosity determined by Core Laboratories, Inc., Wilmington, Calif., for core samples from wells TW-1 and OW-1A Permeability Horizontal Well Laboratory Depth below land Depth below top of (millidarciesl hydraulic conductivity Porosity I sample No. su rface (ttl formation (ftl Air Water mid ft/d (percent) TW-l 1 831.5-831.8 123 1,200 900 0.667 2.19 25.9 2 852.1-852.3 143 676 383 .284 .932 24.3 3 858.2-858.5 149 950 515 .381 1.25 25.0 4 1,137.5-1,137.8 429 870 512 .379 1.25 25.9 5 1,145.6-1,145.9 437 522 287 .213 .698 22.0 6 1,150.7-1,151.0 442 531 243 .180 .591 23.1 7 1,465.4-1,465.8 757 271 148 .110 .360 24.1 8 1,478.7-1,478.9 770 371 200 .148 .487 24.7 9 1,483.6-1,483.8 775 224 156 .116 .380 25.2 OW-1A 10 2,346.3-2,346.5 357 528 256 .190 .623 23.0 11 2,348.2-2,348.5 359 598 324 .240 .788 22.8 12 2,350.0-2,350.2 361 355 206 .153 .501 21.9 1 Twelve core plugs, 1 inch in diameter, and a water analysis were submitted by IPP for use in this study. The 12 core plugs were dried and air permeabilities were determined for each. Each core plug was evacuated and saturated with a simulated injection water synthesized from the water analysis. Specific liquid permeabilities were determined using the simulated injection water. The test results for each core plug indicate that all samples exhibit moderate sensitivity to the simulated injection water. Porosity The values in tables 4-6 indicate that porosity (n) of the Navajo Sand stone in the Red Desert ranges from about 20 to about 25 percent. Assuming that some of the determinations are high, owing to laboratory procedures, the values derived by the Geological Survey--20. 3 to 22.5 percent for effective porosity--appear to be the best for describing the undisturbed Navajo at the test site. The latter values may represent the regional range. G. S. Campbell (written commun., Dec. 2, 1970) reported that the porosity, as read directly from geophysical logs of the petroleum-test well, Mountain Fuel No. 1 State (Bloody Hands Gap Unit), is about 21 percent for the upper 500 ft (152 m) and about 20 percent for the next lower 500 ft (152 m). This well, (D-31 7)36dad-1W, is in the Waterpocket Fold, about 18.5 mi (29.8 km) south of the test area in the Red Desert. Tests on discharging wells Information on the hydraulic coefficients for the Navajo Sandstone in the Red Desert area is based principally on a constant-discharge test at well TW-1. The well was pumped for 35 days, from November 24 to December 29, 1915, after which the recovery of water levels was measured until February 2, 1916. Four wells--ICPA, Stanolind, Colt, and OW-1A--were used as observation wells. The large amount of data for both the drawdown and recovery periods from all these wells was analyzed by a variety of methods described in several of the papers referenced. (For example, see Wenzel, 1942.) The several methods of analysis, which provided a means of cross checking results, ranged from the conventional Theis nonequilibrium-test analysis to simple rule-of-thumb checks, using specific capacity. 19 HVDRAUL IC CONDUCT IVI TV. IN METERS PER OAY o O. 1 O. 2 O. 3 O. 4 0 . 5 O. 6 -,-'1__-,__,-'-,----'--.------, ol----,---'---,-----'----,---r- I - 100 V 6 6 OOV OH 0 0 °H 66 50 200 - >- '"a: ~ '">- - '"~ 300 '" z: '" 100 - z: z: V '" H >- [Q6 6 6 '" oC O 0 >- H oC a: '" a:'" '"~ ~'" ~ 400 - '" ~ l>. V '" 0 ITJH QJ 6 l>. >-'" 0 6 V H 6 6 6 >-'" '"' '"....l '"' ....l'" '" '" x '" >- 150 x l>. >- 500 - l>. '"C '"C 0 Data from tab le Lt 600 0 Data from table 5 - 6 Data from table 6 Horizontal Vertical 200 700 - p 0 H O. 5 1 .0 1 . 5 2.0 20 30 HYDRAULIC CONDUCTIVITY, IN FEET PER DAY POROS I TV. IN PERCENT Figure 9.-Hydraulic conductivity and porosity of core samples from the Navajo Sandstone. 20 In addition to the 35-day pumping test, analysis was made of a part of the data from a stepped-rate production test at well TW-1 made by IPP during September 18-30, 1975. An estimate of T was made for the IePA well from the specific capacity measured during tests made after the well was completed in January 1974. The estimate was interpreted from data reported by R. J. Madsen, February 1974, for pumping periods of 16 to 24 hours. Data for the 35-day test are given in figures 10-14. Figure 10 shows water levels in the Red Desert wells. Note the high artesian pressures; for example, well TW-1 had a pressure of 117.8 ft (35.84 m) above land-surface datum at the beginning of the test, or about 827 ft (252.1 m) above the top of the Navajo Sandstone. Al though the water in the aquifer responds to both barometric pressure and earth tides, the resulting change of water levels is relatively slight. (See fig. 11.) Therefore, because of the large changes due to pumping in water levels in the four wells in the Red Desert, . no corrections were made to these water levels for barometric and tidal changes when they were interpreted for determining aquifer coefficients. In well OW 1A, however, the net change due to pumping was only 2.6 ft (0.79 m), and the water levels were corrected for both interferring effects before determining aquifer coefficients. (See fig. 12.) Graphs of representative test analyse::; are shown in figure 13, which includes Theis non-equilibrium analyses (Ferris and others, 1962, p. 91-103) for the four observation wells, a semilog plot of data using the straight-line method described by Brown (1953), and an image-well distance determination (Ferris and others, 1962, p. 163). These three types of analysis were made for all wells, where applicable. Figure 14 shows analysis of recovering water levels in the pumped well, TW-1. Figure 15 shows analysis of the water levels in the pumped well, TW-1, during recovery from the stepped-rate production test made in late September 1975. In the analysis of the test data, water levels in the observation wells were not corrected for partial penetration, because the radial distances from the pumped well TW-1 to the observation wells were more than twice the thickness of the sandstone aquifer. Because the sandstone is nearly isotropic, the lines of equal drawdown should be vertical, as indicated by Jacob (in Bentall, 1963a, p. 272-282). Transmissivity, as calculated from the observed water levels in the pumped well, is too low because hemispherical flow, rather than radial flow alone, probably occurred in the aquifer close to the pumped well. Well TW-1 penetrated 59 percent of the thickness of the aquifer. Thus, T at the pumped well is more than the calculated value and less than 1.7 times the calculated value. (See following discussion of distance-drawdown analysis.) Results of the several test analyses are given in table 7. The values for T are valid for pumping periods equal to those for which the values were determined, and the values reflect aquifer conditions in the test area. For calculation of long-term pumping effects, a composite figure for T must be used that includes the effects of T in areas beyond the test area. A composite value for T is discussed below. 21 Table 7.--Summary of Discharge: E, estimated. Part of test analyzed: Early recovery, water-level trend that occurred soon after beginning of recovery; late recovery, water-level trend that occurred well after beginning of recovery, generally 2 to 3 days. Source of data: ICPA, Intermountain Consumers Power Association; IPP, Intermountain Power Project; USGS, U.S. Geological Survey Maximum Pumped well Observation Dates Pumping Discharge observed Part of test well period (gal/min) drawdown analyzed (days) (ft) (0-28-8)29dcb-l Feb. 8-9, 1974 0.66 3,110 250' Drawdown (ICPA well) May-July 17,1975 400E Recovery (D-28-8)33bbb-l Sept. 18-19, 1975 1 85 17 Drawdown (TW-l) Sept. 18-30, 1975 12 85-2,150 391 do. Sept. 30-0ct. 11, 1975 Early recovery Late recovery Nov. 24-25. 1975 1 2,800 436 Drawdown Nov. 24-Dec. 29, 1975 35 2,800 512 do. Dec. 29, 1975-Feb. 2, 1976 Late recovery ICPA Nov. 24-Dec. 29, 1975 35 72.5 Drawdown Dec. 29, 1975-Feb. 2, 1976 Recovery Stanolind Nov. 24-Dec. 29, 1975 35 63 Drawdown Dec. 29, 1975-Feb. 2, 1976 Recovery Colt Nov. 24-Dec.29, 1975 35 63.6 Drawdown Dec. 29, 1975-Feb.2, 1976 Recovery OW-1A Nov. 24-Dec. 29, 1975 35 2.6 Drawdown Dec. 29, 1975-Feb. 2, 1976 Recovery 'Recomputed from source given under Remarks, in order to account for artesian head above land surface. 22 results from aquifer tests Generalized Estimated from Computations based on early values (from From straight- SC (for S ~ data (as at points A, fig. 13) points B, fig. 13) line methods 0.0011 Source Calculated of data Remarks T S distance to T S T S SC T (ftl/d) image well (ftl/d) (ttl /d) (ttl/d) (ft) 10-11 2,670 ICPA From data reported by R.J. Madsen (written commun., 1974), for pro duction tests that consisted of two separate pumping periods during two consecutive days. 1,730 USGS From 10-minute recovery after well flowed for approximately 68 days. 5 1,340 IPP During stepped-discharge test. 5.5 1,340 IPP During stepped-discharge test. Specific capacity reported by IPP, as determined from slope of plot of s versus Q. 1,330 IPP Recovery from stepped-discharge test. (See fig. 15.) 1,740 IPP Do. 6.4 2,000 IPP-USGS During principal aquifer test. 5.5 1,340 do. Do. 1,860 do. Recovery after principal aquifer test. (See fig. 14.) 4,200 0.00085 7,190 1,430 0.0019 1,600 0.0014 do. See figures 10 and 13. 4,250 .00093 do. 3,900 .00081 8,200 1,540 .0015 1,580 .0013 do. See figures 10 and 13. 3,110 .0012 do. 2,630 .00055 13,550 1,430 .00063 1,580 .00049 do. See figures 10 and 13. 2,500 .00064 do. 2,630 .0013 do. See figures 12 and 13. 2,630 .0011 do. 23 ~ j iiiI i II Iii iii I II I I III I Iii iii i I Iii iii i I II iii II i I + 6 0 + 5 0 +150 + 40 Colt well +1001 Oistance from pumped well 4,963 feet + 1501 L +30 ICPAwel1 Oistance from pumped well 2,427 feet ~+40 -- +100 + 30 :IE :IE :::> :::> ...... ~ 100 350 1 1 0 Pumping started Pump i ng stopped 400 at 1000 hours 'fat 1000 hours 1 20 IN a v e mb e r 2 4 Oecember 29 1 30 " November 1 975 Figure ID.-Water levels in wells in the Red Desert. +0, +0, +0, -0, >- 3 0, 4 .>- ,"'z .0 z ~o- "'~- ~~~100. ~wo 30. 5 w., "- > ., > w '-" ~ >- z w"''''~"'Z w_ 30.6 w_ ",w", w"'-::> "'ww::>... '" >- ~ >-::E'" "",zc 3 0 , 7 "'" c ",-w "'Zw ::E -::E I aI, a + 180 '"w +0,12 >- w +0, 04", +0.10 c U~ '" ~ +O.03~ +0.08 • oc +0.06 "'- "'-'-" +0,02; 0 o +0.04 ~'" ~ c u + 0, 01 "'- +0.02 o 0 '"w -::E o 0 >- >- >- -0, I w -0.02 w z a ::E >- - w - 0.04 -0,02 "'- >- -0.06 z . .L----4- __ L--<.__ L-...... -._i.. _-,-__ L_ • -0, 03 -120 L,__ -'-_~-'-[)L _ '-----t--;--L- .<-,_...L-,_'--_~--'-_._ L.,,~; __ L_ -0. 08 w 17 20 25 u December 1975 J anua ry 1976 NO TE; Empirical tests show maximum water-level change due to tidal effect lags tidal maximum by 180 minutes for the equivalent water-level change, See right-hand scale. Figure II.-Relation of water levels in well OW-IA to change in barometric pressure and earth tides. 99 . 0 rr",--.rr-rrTl-.-rr-rr-'-lrrlTIT""",rr,TITI",-,rr,TITI"'1'1-"'1"I TIT,rTTT I 1 f IIII,I, j I TTTTTTT'Tlrrrr-rr--.rr-rrTlrrrrT-r--.rr-rrTl"'-rTT"l-.-n 3 a. 2 30.3 >- >- z z 30,4 0 0 "- "- nonpumping level '-" 1 0 0 . 0 '"z z 3 0 . 5 ::>'" '"::> ~ ~ c c 3 6 w w a. ::E ::E ,., Smoothed drawdown' ':-'\2-- Mea sur e d wa t e r I eve I •0 0 ~ ~ \ 30. 7 w w '" '" '\ 1\ .... 1 0 I , 0 Distance f rom pumped wei I, 25.185 feet '" w '. v \ 3 a. 8 '"w w (See note in figure 10) ,I >- "'- w Water levels from diurnal tape measure "I Wa t e r I eve leo r r e c ted for :a; ments and cant inuous-recorder graph bar 0 met ric and ear t h • tid a I "\f""'-/' 30. 9 I" ... ~ effects \\'-1'1 / '"w '-\1'. (\ >- \ "". I \ / 31 . 0 '"w c I ... ,., \\-j--.\ c 0 \ ''\----., / • >- 102.0 \ ,~-\-.( 31 . 1 0 No >- :I: \ \/ > r e cor d :I: " ...... >- w "- o Pumping started Pumping stopped \ 31 . 2 w at 1000 hours at 1000 hours \'C--Extrapolated drawdown 0 November 24 Oecember 29 \ 31 . 3 ~ / \\ J I 03. 02,L!-'-":2:-'5,LLl.-4 ...L~l...1..LJ""ILO:-'-.Ll..JI""5~.LJ.~2:-'0:-"-LL~2~5...LL..U.LJ.-f:l-~' II '1 ~ II '; I '~1~-'-'--'2--'5~-'-'-"""'+L.'-~:'-L.L-'-'-1-:0-'--'L.L"-1.L5"""'....L.2-'-'-0..w....L2'---'-'5 3 I 5 November Oecember January February 1 975 1 976 Figure 12.-Water levels in well OW-IA. 25 We II W(u). u ~ (0-26-8 )29dcb s '" Z (ICPA) tlr '" Match pOint. +6 ~ y Mat c h poi n t A A: r o2l2..c0oo x [.0 1 af------~F_'O-_+-_,t'_-- - 4- x [0. 2 '" 4,200 ft 2 /d (390 mZ/d) S = 4 x 4,210 x 5.05 x 10-8 8.) x 10-4 \ 8:r 222...L.QQQ x l.O T ypee u r v e 4Trx 29.9 W(u), u '" LO 1,430 ft;~/d (390 m2 jd) ~ s '" 10.2 4 x 1,430 x 3.28 x 10- 7 ~ Z t/r '" 5.05 x 10-8 1.88 x 10-3 ~ l-_-L-l-l---.L-lIJIJI.LIl..!__L--_LI_LI-L1JI..lJ..lL_--l_-"----"---L.L..L.LJ...L a. 3 ::E z (t/r Z ) Z z ,. z C> ,. C> C> ,. C> 4: ,. 0: 4: C> 0: C> "-0 2l2~ x 1,0 41)xl1 '" :3,900 ft 2 jd (302 mZ/d) S ",·4 x 3,900 x 6.2 x 10-8 Type curve :0 8.1 x 10-4 \ B: r ""' ;539,000 x 1.0 f+1rx27.8 W(u), ~: ii O 1,540 ft 2 /d (143 m2 /d) 7 t/r Z '" 6.2 x 10-8 4 x 1,540 x 2.38 x 10- 1.47 x 10-) __.L-L---.L...L.11-L1-L1.L1LI__-LI_-LI-lI-L-LJ..li.L_.-J_...L-L-LUllL L 0.3 (tr lrr 2 ) ...... z Image distance: At Sr =: Si 10 ft t r /rr 2 '" 2.02 x 10- 7 z 2 10 ti/rr = 1.4 x 10-6 r i = rr Ifi7Il- ...... "" 3, 11J /1--r:-5677l.-958 0: 0: ::l ::l '" 8,200 ft (2,500 m) ...... 0: 0: 4: 4: a.. a...... C> C> 1'-_~.J...-LL.LJ..l-'-L_-'---.l.---L..L...L-L.LJ.-L __.L..-.L-..L...LJJllt 10-6 10-7 (ti/ rr'l 10-6 10-50. t/r z • IN DAYS PER SQUARE FOOT 2 t/r J IN DAYS PER SQUARE METER Figure 13.-Representative data analyses from 3S-day aquifer test. 26 St raj g h t - lin e met hod a n a I y s i _s_--~-----r---r-r-'--'--'--T>- (t/r'lo o-;,-=:~~-,~ We II (0-28-8)29dcd-1 ( ICPA) 20 o 0 0 0 ~ " 25.2 o / (I) 000 >- '" 000 10 '" '">- '"~ '"::E 40 _ 2.303Q - 411,'..5 = 2.303x539,OOO 15 z 4':'"(86. ')-25. 2) 1,610 ft?/d (150 ml/d) z 0• (t:/r~) •0 0 60 2. 1ST 0 • '" 1.25 x 1,610 x \,1'14 x lO-7 .. 1.]9 x 10-) 20 ..• '"0 '"0 80 s '" 86.5 25 30 10-5 t/r2 • IN DAYS PER SQUARE FOOT 10-6 1 0 -- 4 t/r Z • TN DAYS PER SQUARE ME11:R Pwnped well: (D-2B-8)33bbb-l Q = 2,800 gal/min (176.7 = 539,000 ft'fd (15,270 Distance (r) from pumped well: (D-28-8)29dcb-l 2,427 feet (740 m) 29cdc-l 3,113 feet (949 m) 33cdd-lS 4,963 feet 0,513 m) (O-27-8)27cdb-l 25,185 feet (7,676 m) "'- 0.1 1.0 = 1.63 "" 1.21 x 10- 7 Theis non-equilibrium analysis (I) r-----,,--,,---,-rn-rr--r------,-----,-"TTT,-----',----,---rr-rrrn- 3 0 0.3 '" >-'" ~ ::E z z 1.0 z s '" 30.0 z t/r2 = 1.1 x 10- 7 z •o .- 539.000 x 1.0 z o 0 4~16. 3 • .-0 2,630 ft2/d (244 ro 2 /d) .. z '" 0.03 .. S = 4 x 2,630 x 5.2 x 10-8 o '"0 o• = 5. 'j x 10-4 o T '" 539,000 x 0.1 • 41T x1.63 .. 2 '= 2,630 ft2/d (244 m /d) '"o S '" 4 x 2.630 x 1.21 x 10- 7 (133 m? fd) "" 1. 27 x 10-3 Type 1. 1 x 10- 7 1~-~~~_LJ-U..LLc::----'-_~-'--'~L.U-'-_~---'----'-~.L.LL4. 0 o. 01 O. 003 10-8 10- 7 10- 6 10-5 ' 10-8 10-7 10- 6 t/r2 ~ IN DAYS PER SQUARE P?OT t/r 2 , IN DAYS PER SQUARE FOOT 10-6 10-5 1 0- 4 10-7 10- 6 10-5 2 2 t/r , IN DAYS PER SQUARE METER t/r , IN DAYS PER SQUARE METER Figure 13.- Continued. 27 10 50 20 ...... Time increases since pumping 100 slopped 30 40 '" :: 1 50 ...."" .... I- ... 50 .... z '''·,1 '" -:J 60 z ·20 0 ~ ~ f '-, = 2,800 gal/min (176.7 l'"~ N 00 '" 539,000 ft~/d (15.670 1 c ...... 80 2~:~:Q (~ ~) . t c T = log x t. :::> "' c !""t ... - :::: 30 ot 2.303 X 539,000 x 1 . J90 ....'" "" 4""(115-62) ... . ~ '" 1,860 ft 2 jd ... . j- 1 00 The expression x ~ is a correction for an interruption in pumping .. 35 0 f- * .. 1 1 0 if'!. which, t l = time since first pumping step started, t': time since first pumping step stopped, time since second pumping step started, t'l" = time since second pumping step stopped 400'- " 1 20 1 30 45J IIIII III IIII III IIII III IIII III III IIII I'III J 1 10 10 2 10 3 10 4 105 10 6 (~ x RATIO OF TIMES I't\ Figure 14.-Analysis of residual drawdown in well TW-I after pumping for 35 days. '" [) '" t90 ~c 50 2,BIO 50 s '" 7S 3,890 --1 25 100l ______B ;" . Gage error ~ .". '" c ' .. '">- ••~S 150 •• =: 6. S85 '" : 15aL .. '"' ...... z . 50 z ~ ~. ~ " '"c . ..~ N '"c \.0 i,320 ...... ::> c T '" 35.29 x 8,845-7.320 - 300- 200 \ -A '" '" i'+r 538 ftl/d \ f r '" 35.29 x 6,585-2.810 \ I 150-50 I '\\' 7 5 250 = 1,330 ftl/d T '" 35.29 x 3,890-190 75-0 1,740 ftl!d where, T '" ~ log t;, t'J ft 2 jd " 300 where Q is in gallons per minute, S ,845 300 and t:= time since pumping started, t' '" time since pumping stopped 1 00 3 5 0 1 1 1 1 1 I 1 I I 1 1 o 1000 2000 3000 4000 5000 6000 7000 8000 9000 VALUE OF TIlE TER!1 Q. log ~ Q, log~- - Q log rio + t' lC t2 + t' ' t3 + t' t' Figure 15.-Analysis of residual drawdown in well TW-I after pumping for II days at increasing rates of discharge. The analyses indicate that the Navajo Sandstone, though nearly isotropic in undisturbed cores, is grossly anisotropic where it has been fractured. Moreover, the Navajo aquifer is heterogeneous. For example, three of the log log plots in figure 13 show that an apparent boundary appears in the early test data, utilizing a match to the Theis type curve at points A. Departures from the type curve suggest a line beyond which, or along which, the aquifer has lower permeability than it has near the wells. The loci of the line were calculated using the graphic method of Moulder (in Bentall, 1963b, p. C110 C112). The trend of the line appears related to geologic trends in the area, although no direct surficial feature is evident. Assuming that the apparent change in T has only a transitory effect on the long-term development of the cone of depression, the points in the three log-log plots can be generally matched at points B. These matches yield lower and more uniform values for '1'. Straight-line semi-log plots of the observation-well data also indicate the effect of the changes in value for as the cone of depression spread. The example in figure 12 shows a straight line fitted to the data, but it also should be noted that the trend of points is curvilinear. For an isotropic formation, the data should have approximated a straight line after a maximum of 17 days of pumping--after which the value l/u is greater than 50 (Brown, 1953, p. 858). However, the image-well effects arrived before that time, as shown in the Theis non-equilibrium analysis for the same well. Because of the seemingly conflicting values for T , the drawdown in pumped well TW-1 was corrected for partial-penetration effects, and the drawdowns in the pumped and observation wells were plotted versus distance. (See fig. 16.) The resultant value for T is 2,560 ft2/d (238 m2/d). This value is in the range of those for T determined at match points A in the curves for the observation wells. Transmissivity 2 A generalized value for transmissivity '1' of 1,500 ft2/d (139 m /d) is selected for calculation of long-term pumping effects in the fractured Navajo Sandstone aquifer near Caineville. The selection of the generalized value was made after considering the following factors: 1. The generalized values for T (table 7) correspond closely. 2. All values of T obtained from the tests (table 7) are higher than any based on values of K determined from the cores. This indicates that secondary permeability, probably the result of fracturing, has an important effect on well yields and water-level response to pumping. Such response would be most affected in the areas of maximum aquifer distortion near the crest of the Caineville anticline; but cross fracturing might also be present, due to the plunge of the anticline, both northward and southward. 3. The time-drawdown curves show a "discharging-boundary" response. This boundary effect is real. It appears in the plots for all wells in the Red Desert, in both the drawdown and recovery curves. The boundary plots to the north of the well field, and it either parallels or intersects geologic features that indicate structural distortion. 30 Nothing constituting a zero-permeability barrier is evident from the surface geology, but the response is reasonably sharp. From the responses observed, it is inferred that the boundary represents a line along or beyond which T is less than in the well field. Thus, the generalized values for T derived from match points B (table 7) represent a composite response to conditions in both the area of high T near the wells and the area beyond the boundary where a lower T occurs. 4. The T at well OW-1A is in the same range as that at the wells in the Red Desert (table 7). It appears, therefore, that fracturing affects substantial areas of the sandstone aquifer, and that nowhere is it likely that T, as determined from wells, will be as low as that calculated from core permeabilities. Thus, the generalized value of 1,500 ft2/d (139 m2/d) is considered to be the most useful value of T for computation of long-term pumping effects in the Navajo Sandstone aquifer near Caineville. Iii III I ,------r-n, 1----- 2.3Q loglOr Stanoli~d ~ T = 21T(sl-s2) ICP~Olt -25 2.3 x 539,000 x 1 100 2 x 1T x (254-177) 2,560 feet squared per day ~~ ~~ -50 s2 = 177 0- '" 400 = 331 feet l/C " 1 + 7(rw/2am)"cos(1Ta/2) -1 25 1- Where rw = radius of well = 1 foot m = full thickness of formation = 911 feet Observed drawdown 9ll)~ -1 50 500 507 feel al wei I TW-l l/C = 1 + 7(1/0.59 x COS(1T x 0.59/2) 1..107 '----__-'-----_L----'------L_--"----L-L--'--L '------'_--'-----"-----'----'~~__L- I ! IIII 1 0 1 0 2 OISTANCE FROM PUMPEO WELL. IN FEET , , --,------,,----- O. 5 10 I 0 2 10 3 OISTANCE. IN METERS Figure 16.-Drawdown as a function of distance from well TW-I after pumping for 30 days. 31 Storage coefficient A generalized value of 1 x 10-3 for storage coefficient (5) is selected for calculation of long-term pumping effects in the Navajo Sandstone aquif~~ near Caineville. The calculated values shown in table 7 range from 4.9 x 10 to 1.9 x 10-3, but these values were derived using values of T that are too large. The selected value is estimated to be a fair compromise. It checks against an approximation of 5 using the rule of thumb cited by Lohman (1972, p. 53), which is based on ~he more precise method of Jacob (1950, p. 334). The approximation is 9 x 10- , which is based on a formation thickness of 900 ft (274 m) that is multiplied by 1 x 10-6 . The selected generalized value for 5 is high for a confined aquifer. It is probable that some dilation of the aquifer occurs because of the high pressure, and this leads to compaction when pressure is relieved by flow or pumping. Evidence of compaction seemingly is given by the water-level changes in well (D-28-7)36bbb-l during the 35-day test. (See fig. 17.) The water level in the Navajo Sandstone beneath this well was at an altitude of about 5,040 ft (1,536 m), as projected 2.5 mi (4 km) upgradient from well (D-28 8)29cdc-1. Well (D-28-7)36bbb-1 on the same date had a water-level altitude of 5,119 ft (1,560 m) or about 80 ft (24 m) higher than that in the Navajo. Despite the approximately 1,400 ft (427 m) of strata that separate the Navajo from the Salt Wash Sandstone Member of the Morrison Formation in which well (D-28-7) 36bbb-1 is finished, water levels in the well apparently declined in immediate response to withdrawals from the Navajo. ThUS, it is inferred that the Navajo compacted. ...... 5.6 :;: ...'-' ...... 1 8 C< C< ::> ::> en en 5 . 4 We 11 (0-28-7 )36bbb-1 c c Aquifer: Salt Wash Sandstone Member z z ...... of Morrison Formation 5 . 2 ...... 1 7 AlIi tude: 5.100 feet (1.555 meters) ... Alt itude of highest water level ...,.. ,.. c c before pumping of wei I TW-l: 5.119 feet ...'" (1,560 meters) 5.0 : .... 16 L....-'-~--...-'--'--...... -'-~'---'--'- ...... --'-_...... --'-_...... J.--'-_~~ ...... -'- <-I.-'-~--...-'-~ -'-~.....:I ~ ~ 1 5 ...... -.-...... ---r-.-...,...... ---T"-.-..,..-,,...... ,...-.-..,..-,,...... ,...-.--r-"'O-..---r-...... -..---r-~...... ,....~~-.- .-r-.-...... ---r-.- .---r-.-...,...... , 2 2 :: z 20 :E - 60 Z en- 16 . .... en ...,.. 45 .... 12 ,...... Wei I (0-28-8)29cdc-1 ...... Aquifer: Navajo Sandstone ... C< .... AI ti tude: 4,940 feet (2,350 meters) ...... Altitude of highest water level ...... • 15 before pumpina of well TW-l: 5,006 fee t 4 • (1,525 meters) 1974 1975 1976 1977 Figure 17.-Water levels in wells (D-28-7)36bbb-1 and (D-28-8)29cdc-1 emphasizing changes during 35-day pumping test. 32 Long-term pumping effects If the Navajo Sandstone were used as a source of cooling water for a powerplant, withdrawals would be large and of long duration. The areal effects would depend on factors such as the number and location of supply wells, the rate of pumpage, the location of aquifer boundaries, and changes in T at different sites that would be due to formation thickening or thinning. An example of long-term effects is given in figure 18, which shows a set of simplified conditions and assumptions. The figure shows that if well TW-1 were pumped at 3,000 gal/min (189 L/s), the water level in the well would still be 73 ft (22 m) above the top of the aquifer after 40 years of pumping. Near Hanksville, 18.9 mi (30.4 km) to the east, the pressure in the Navajo Sandstone would have declined about 50 ft (15 m). Since boundaries and areal changes in T do exist, the actual drawdown from pumping 3,000 gal/min (189 L/s) would be somewhat greater, and adding other wells to the pumping system would create mutual interference. The additional drawdown due to these effects would increase drawdown at well TW-1j and after 40 years of pumping, the water level would have declined below the top of the Navajo Sandstone. oI STANCE FROM WELL TW-l 1 0 1 00 1000 1 0 , 000 100,000 FEET 1 0 100 1000 10,000 METERS III I -25 1 00 -50 75 ...IX'" I-... :IE 1 00 -z z •0 0 -125 c• IX 0 -150 Assumptions: Cont inuous pumping of well TW-l only. No boundaries or Changes in T. After 40 years pumping, drawdown T = 1,500 feet squared per day -1 75 600 at distance of 1 foot is 754 feet, S=IXl0-3 or 73 feet above top of the Navajo a = 3.000 gallons per minute, or Sandstone 4,820 acre-feet per year - 200 0.01 0.1 1.0 10 KILOMETERS ~, ---J----LL.~-T-'---'---'--.L.L.- 7 0 0 -----'---'--',-I-"-'1-1--'-'-1-' ..J...I...LI...L1 L-----lI..lI---.L1----1.1'I.1.1.JI-LI1-11-1 _ ___'_ ____I._L_.1.._.l,_Lll--.LLj 0.01 0.1 1 .0 10 18.9 MILES DISTANCE FROM WELL TW-l Figure 18.-Theoretical effect of long-term pumping at well TW-I. 33 If the water level were to decline below the top of the Navajo Sandstone, water would then be obtained from storage by draining pores, at a rate of release greatly exceeding the rate of release under confined conditions. For a given rate of discharge, the rate of development of the cone of depression would then diminish. The specific yield is estimated to be between 5 and 10 percent, or at least 50 times greater than the amount of water released from artesian storage. Water-level declines of the magnitude implied probably would result in a change in the chemical quality of the pumped water for two reasons. First, pressure relief probably would induce upward leakage from formations that underlie the Navajo Sandstone. Secondly, if the water level in the Navajo were to decline below the water levels in the Carmel Formation, drainage from that formation down to the Navajo would occur. In both cases, the chemical quality of the pumped water would be degraded. The amount of potential degradation is unknown, but it is inferred that the quantity of leakage would be small and thus the degradation also might be small. CHEMICAL QUALITY OF GROUND WATER Extensive sampling was done on well TW-1 during the 35-day pumping test, on the Colt well while it was being converted to an observation well, and on the ICPA well while it was being drilled. Selected chemical analyses from this suite of samples and from other sources in the test area are given in table 10, and a record of discharge measurements during sampling, ground-water temperature, and specific conductance are given in table 11. The chemical analyses support the inference that ground water moves from one aquifer to another. Based on the chemical data and on geologic and water level data, it appears that the most probable avenues of movement are fractures due to folding. These conclusions follow from the discussion below. The Navajo Sandstone consists mainly of quartz grains with little interstitial cement. Thus, water moving through it, despite long residence time, should not be appreciably mineralized and would be of the calcium bicarbonate type. The Carmel Formation, which overlies the Navajo Sandstone, contains large amounts of gypsum; and to the north and west of the test area, contains salt (Gilluly and Reeside, 1928, p. 74). Thus, the Carmel could yield water of the calcium sulfate or sodium chloride type. The Kayenta Formation, Wingate Sandstone, and Chinle Formation directly underlie the Navajo Sandstone. The Kayenta and Chinle contain shale beds, and the Wingate is of lower permeability than the Navajo. Thus, the section un derlying the Navajo could be a source of water that is more highly mineralized than the water in the Navajo. Water under artesian pressure in deeply buried aquifers in the Red Desert area could discharge upward from deeper formations to shallower ones along fractures due to folding. Although the leakage under natural conditions might be small, the rate of leakage could be increased by withdrawals from the system. 34 The analyses of water samples from the Colt well (table 10) give a verticle profile of the chemical quality of water at that location. A sample of water that flowed from the open hule (table 8) on July 14, 1975, contained 7,210 mg/L of dissolved solids (table 10) and was of the sodium chloride type. This sample may have included water from all formations between the Chinle and Carmel Formations, inclusive. All samples later obtained from the Navajo Sandstone and the Carmel, however, contained a considerably lower dissolved solids concentration. Because water pressures increase with depth, it can be inferred, therefore, that the highly mineralized water came from beneath the Navajo. Near the middle of the Navajo Sandstone, (1,286-1,296 ft or 392-395 m) the water contained 1,170 mg/L of dissolved solids and was of a mixed type, with sodium and chloride as the dominant ions. About 150 ft (46 m) below the top of the Navajo, the water contained 740 mg/L of dissolved solids and was of a mixed type. At the top of the Navajo, the dissolved-solids concentration was 964 mg/Lj and the water was of the mixed type, with calcium and sulfate as the dominant ions. The base of the Carmel Formation (sample from 663-673 ft or 202-205 m) yielded water similar to that at the top of the Navajo, but water from higher in the Carmel (sample from 611-621 ft or 186-189 m) was again more mineralized. Thus, upward leakage from the Navajo to the Carmel is implied. The ICPA well was sampled while it was being drilled. The uppermost sample was obtained from the Carmel Formation when the well was flowing and was 597 ft (182 m) deep. The dissolved solids were 4,580 mg/Lj and the water was of the mixed type, with calcium and sulfate as the dominant ions. Water from the uppermost 20 ft (6.1 m) of Navajo Sandstone in the well was slightly more dilute but contained more sodium than calcium. A composite sample from the Navajo when the well was 761 ft deep and had penetrated 93 ft of the Navajo yielded a still more dilute mixed water with sodium as the dominant ion. The artesian pressure is greater in the Navajo than in the Carmelj thus, it appears that water moves upward from the Navajo into the Carmel, where it is degraded in chemical quality. Well TW-1 penetrates 546 ft (166 m) (about 59 percent of the total thickness at this well) of the Navajo Sandstone. Pumping the well for 35 days had relatively little effect on the percentage composition of dissolved constituents, and the chemical quality was almost uniform from one sampling date to the next. The water was of the sodium chloride sulfate type. It is believed that water from well TW-1 in part leaks from formations below the Navajo, and that given a large lowering of head due to pumping, the water probably will deteriorate to some extent with time of withdrawal. The only other water samples available from the area of the test near Caineville are from the Salt Wash Sandstone Member of the Morrison Formation. A sample from the Clark well, which is 800 ft (244 m) deep, had a much lower dissolved-solids concentration than did samples from the deeper Carmel Formation tapped by other wells. Water from the Clark well was of the sodium sulfate type and had a relatively low chloride concentration. Leakage from below does not affect the chemical quality of water in the well because the water is perched above the potentiometric surface in the Navajo Sandstone. 35 CONCLUSIONS The Navajo Sandstone near Caineville :is a massive, crossbedded, very fine to fine-grained unit, approximately 900 ft (274m) thick. The un fractured sandstone, for the practical purpose of aquifer analysis, is hy draulically isotropic. It has an average K of about 0.5 ft/d (0.15 mid), with an average horizontal-to-vertical permeability ratio of 1.42: 1. The 2 calculated T, based on the above value is 450 ft2 /d (42 m /d). Folding of sandstone has produced fracturing that probably facilitates some interformational leakage. The leakage, under natural conditions, is up ward under a high artesian head. The fracturing has increased the overall permeability so that the formation is heterogenous and probably anisotropic on a regional scale. Con ventional aquifer-test analysis, assuming an isotropic formation, does not yield the uniform results that might be expected from the relatively homo geneous sandstone. Based on both time-drawdown and distance-drawdown analyses, a gener alized v!lue for T selected for calculation of long-term pumping effects is 2 1,500 ft Id (139 m /d) or 3.3 times that calculated for the unfractured forma tion. A generalized value selected for S is 0.001 under artesian conditions. For water-table conditions, the value for 8y is estimated to be between 5 and 10 percent. Natural interformational leakage in the test area is inferred from chemical, geologic, and water-level data. It also is inferred that some degradation of the chemical quality of the well water would be induced by large withdrawals from the Navajo Sandstone. Initially, this increase in min eral content would be due to upward leakage from underlying formations under high artesian head because of the large pressure drop within the Navajo. If water level in the Navajo were to drop below the water level in the overlying Carmel Formation, water would drain downward from the overlying Carmel. In summary, the Navajo Sandstone near Caineville is capable of sus taining large yields of slightly saline water to wells for periods of many years. Drawdown near pumped wells would be large, and the effects of pumping would extend to distances of 20 mi (32 km) or more. 36 REFERENCES CITED Baker, A. A. 1946, Geology of the Green River Desert-Cataract Canyon region, Emery, Wayne, and Garfield Counties, Utah: U.S. Geological Survey Bulletin 951. Bennett, G. D., and others, 1967, Analysj.s of aquifer tests in the Punjab Region of West Pakistan: U. S. Geological Survey Water-Supply Paper 1608-G. Bentall, Ray (compiler), 1963a, Methods of determining permeability, transmissibility, and drawdown: U. S. Geological Survey Water-Supply Paper 1536-1. _____1963b, Short cuts and special problems in aquifer tests: U.S. Geological Survey Water-Supply Paper 1545-C. Brown, R. H., 1953, Selected procedures for analyzing aquifer test data: Journal of American Water Works Association, v. 45, no. 8, p. 844-866. Feltis, R. D., 1966, Water from bedrock in the Colorado Plateau of Utah; Utah State Engineer Technical Publication 15. Ferris, J. G., Knowles, D. B., Brown, R. H., and Stallman, R. W., 1962, Theory of aquifer tests: U.S. Geological Survey Water-Supply Paper 1536-E. Gilluly, James, 1929, Geology and oil prospects of part of the San Rafael Swell, Utah: U.S. Geological Survey Bulletin 806, p. 69-130. Gilluly, James and Reesi de, J. B., Jr., 1928, Sedimentary rocks of the San Rafael Swell and some adjacent areas in Utah: U. S. Geological Survey Professional Paper 150-D. Hunt, C. B., as.cdsLed !)aul J1ver'iU ard !i.L. ;"!7'lZ Y', 1953 Geology and geography of the Henry Mountains region, Utah: U. S. Geological Survey Professional Paper 228. Jacob, C. E., 1950, Flow of ground water,,'n Rouse, Hunter (ed.), Engineering Hydraulics: New York, John Wiley, p. 321-386. 1963, Correction of drawdowns caused by a pumped well tapping less than ----- the full thickness of an aquifer, /n Bentall, Ray (compiler), 1963, Methods of determining permeability, transmissibility, and drawdown: U.S. Geological Survey Water-Supply Paper 1536-1, p. 272-282. Lohman, S. W., 1972, Ground-water hydraulics: U.S. Geological Survey Professional Paper 708. 37 Lohman, S. W., and other, 1972, Definitions of selected ground-water terms-- revisions and conceptual refinements: U. S. Geological Survey Water- Supply Paper 1988. Smith, J. F., Jr., Huff, L. C., Hinrichs, E. N., and Luedke, R. G., 1963, Geology of the Capitol Reef area, Wayne and Garfield Counties, Utah: U.S. Geological Survey Professional Paper 363. Stokes, W. L. (ed.), 1964, Geologic map of Utah: Utah Univ. Wenzel, L. K., 1942, Methods for determining permeability of water-bearing materials, with special reference to discharging-well methods: U.S. Geological Survey Water-Supply Paper 887. Williams, P. L., and Hackman, R. J., 1971, Geology, structure, and uranium deposits of the Salina quadrangle, Utah: U.S. Geological Survey Miscellaneous Geological Investigation Map 1-591. 38 T Locati.on: See text for description of w!.'tt- and spring-numbering system. W(·ll finish: P, perforated; X, open hole. Watl'r lev!.'l: R, Oi seharge: E, H, reported. lJrawdown: E, estimated. R"'marks and other data avai.lahle: - fl, common dissolved l;onstituents, and H, multiple (tabLe La), K, specific conductance and temperature (table 1 l); - L, dritter's or oj (tahle 9), G, geophysical 10.11; in files of Surveyor owner; Water levels - WL, hydrographs in figures la, 12, Of 17 mensurement s in file S 0 [ Ceo logic II I Surv,'y. Altitude Water level Depth of land- (feet above Date Name OWnPf Ycar con- ol Wpl.l surface or below(-) Date Drawdown discharge Remarks and other data available Location '''': (D-28-7) llcdh-SI Rock Water Spring 5,430 Discharges from Salt wflsh Sandstone Member of the Morrison Formation in bluff at :'IOuth side of Hartnet Draw. II. 27cdb-l IF\' observation well 1975 2,351 5,162 -94.7 9-23-76 30Of<: 11-20-75 Observation well drilled for aquifer test. (OW-lA) Drilled to 2,341 ft; cored to 2,353 ft. Casing: 6-io. to 42 ft; 5-in. 42-1,990 ft, stage-cemented from 1,990 ft to land surface. Developed by jetting and 7 hours of air-lift pumping. Equipped with auto matic water-level recorder for duration of project. M, L, G, WL. 36bbb-l Emmett Clark and 1966 BOD 5,100 30R 7-14-66 3.5R 7-14-66 Flowing stock well on east side of North others l7.B 7-17-75 1.9 7-17-75 Blue Flat. Finished in Salt Wash Sand stone Member of the Morrison Formation. Flows continuously to stock trough. l.eaks around surface casing. Casing: lO-in. to 330 ft; B-in. from land surface to 726 ft. B, L, WL. (D-2B-B)29cdc-l Stanolind 1955 764 4,940 168 4-13-74 100R 8- 7-55 Flowing stock and wildlife well. Flows con (Red Desert) 55.3 3-17-76 48 3-17-76 tinuously to pond. Originally drilled to 61.8 3-31-77 47 3-31-77 supply oil-test well. Casing: 13-1n. to 32 ft; 7-in. from land surface to 720 ft. Top of sand in base of Carmel Formation at 693 ft; top of Navajo Sandstone at 720 ft. (See p. 12.) M, L, WL. 29cdc-2 Stanolind Oil Co. 1955 7,160 4,936 Abandoned oil test. Drill-stem test in No. 1 Federal Mississippian limestone, 6,556-6,618 ft re covered 6,125 ft of reportedly freshwater. L. 29dcb-l ICPA test well 1974 761 4,896 69R 4-13-74 3, nOR 1 250E 1 2- 9-74 FlOWing test well. Shut in after tests by 108.0 11-24-75 4001: 7-17-75 IPP. Casing: 20-in. to 22 ft; 16-1n. from 90,0 2- 2-76 2.4 ft above land surface to 679 ft below land surface, cemented to shut off flow from Carmel Formation. M, L, G. WL. 32acb-l Ohio Oil Co. No. 1 1922 3,650 4,990 Abandoned oil test. L. Federal 33bbb-l IPP test well 1975 1,250 4,884 117.8 11-24-75 2,800 511 .S? 12-29-75 Flowing test well. Drilled 9.6-in. pilot OW-I) 107.0 3-l7-76 hole to 1,685 ft; cored three intervals. 114,1 5-10-76 (See table 3.) Plugged 9.6-in. hole back 121.6 7-22-76 to 1,250 ft. Casing: 3D-in. to 45 ft; 20-in. from 2 ft above land surface to 704 ft below land surface. All casing cemented to formation to isolate Navajo Sandstone and seal in the artesian head. Producing section, 704-1,250 ft, is l8.5-in. open hole. M, L, G, WL. 33cdd-lS Colt well 1975 1,350 4,823 177.2 11-11-75 8- 5-75 Flowing observation well. Originally drilled 178.4 11-24-75 8-21-75 to 3,700 ft as an oil test by Colt oil Co. l70.0 3-31-76 :In May 1975. Re-entered by IPP in August 176.7 5-10-76 1975. Original casing record: 13.6-in. to 182.5 7-22-76 100 ft; 8.6-in. from land surface to 1,400 ft. Open hole to 3,700 ft, drilled to 7.9 in. diameter. Oil test reportedly plugged at 3,475-3,700 ft, 2,425-2,500 ft, and 1,350 1,400 ft. On re-entry, no plug found ahove 2,425 ft and casing found to be poorly ce mented. Conversion to observation well started with plugging below 1,350 ft, and stage-cementing casing to completely seal off Navajo Sandstone and Carmel Formation. Five 10- ft zones were gun-perforated for drill-stem testing, using straddle packers. A sixth zone was later added to test the basal Carmel. After testing, well was com pleted by squeeze-cementing all perforations nbove 756 ft [lnd increasing the perforations to include a total of 130 ft within the zone 756-l,296 ft. (See sampling zones listed in tableR 10 aod 11.) M, L, G, WL. 35hca-Sl Seep 4,600 3-25-76 Intermittent spring. Water probably is under flow in alluvium upstream, which is brought to the surface by convergence of the base of the alluvium wi.th the streambed. On March 25, 1976, temperature was 11 °C; specifi.;: con ductance WaS 6,500 micrornhos. K. lAfter production pumping test; drawdown recomputed from value reported by R. J. Madsen (written commun., 1974) to account for artesian head above land surface. 2 After pumping for 35 days . .JOischarge through 50 ft of perforations, prior to observation well completion. (See table 11.) 4 Discharge through 130 ft of perforations after ohservation well completion. 39 Table 9.--Selected logs of wells Location: See text for description of well-numbering system. Altitudes are in feet above mean sea level for land surface at well. Thickness, in feet. Depth, in feet below land surface Material Thickness Depth (D-28-7)27cdb-l. Summarized from sample logsl by W. G. Hannah, T. P. Condiff, and L. A. Jackson, Los Angeles Department of Water and Power. Alt. 5,162. Brushy Basin Shale Member of the Morrison Formation 2 Sandstone, fine- to medium-grained, soft, massive.••..... 10 10 Sand, fine- to coarse-grained, varicolored, with 30 per cent claystone chips; firm and greenish claystone, bound the drill string between 30 and 40 ft •.••.•••.•.. 30 40 Sand, varicolored, fine- to coarse-grained. •.••••••••.••• 10 50 Claystone, firm, greenish-gray to reddish-brown.•••....•• 20 70 Claystone, gray to reddish-brown, soft and sticky to firm; sandy in some zones, and with agate chips at 100 to 160 ft . 180 250 Claystone, brownish-purple to gray and green••••.•..••..• 10 260 Claystone, gray to brown, soft to firm chips ••••.•.•••••. 30 290 Siltstone, sandy to clayey, red-brown, sticky, and very fine grained sand; rough drill action 303 to 305 ft •••• 20 310 Salt Wash Sandstone Member of the Morrison Formation Sandstone, brown, very fine to fine-grained, with trace of gray claystone . 10 320 Sandstone, light-gray, fine-grained, with coarse, angular fragments that may be cavings ••••.••..•...•.....•.••••• 10 330 Sandstone, gray, fine- to coarse-grained, hard, with red agate chips and other rock fragments •...... •.•••...••.. 10 340 Sandstone, gray, fine- to coarse-grained, hard, and chips of brown claystone and grayish-green siltstone••.•••••• 75 415 Siltstone, claystone, and fine-grained sandstone, reddish-brown . 15 430 Siltstone, claystone, and sandstone, light to dark gray with some red-brown..•.•.....•..•..•.•....•.•••...••... 10 440 40 Table 9.--Selected logs of wells--Continued Material Thickness Depth (D-28-7)27cdb-l - Continued Salt Wash Sandstone Member of the Morrison Formation - Continued Sandstone, gray, fine- to coarse-grained, hard, cal careous, subangular; hard drilling...... •...... •. 15 455 Siltstone and claystone, red and green, feldspar, slightly calcareous gray shale, and fine-grained sandstone ...... •..••.•...•...... •.. 15 470 Siltstone and claystone, and gray fine- to medium- grained sands tone...... •...... •••...••••.....•.• 10 480 No record .....•...... •.....•...... •..•...•..... 10 490 Sandstone, very fine to fine-grained, siltstone, and gray calcareous claystone, and green to red clay- stone . 10 500 Siltstone and claystone, greenish-gray and reddish brown, soft to firm, fine-grained calcareous sand stone, and trace of red agate; zone 510 to 515 ft drilled fast; zone of siltstone and claystone 520- 530 ft is soft; cuttings break down in water••••••.•... 40 540 Sandstone, fine- to coarse-grained, calcareous; mainly in grains 540 to 550 ft and firmer, with cemented chips 550-555 ft; 10 percent red to green claystone•••• 15 555 Summerville Formation Claystone, siltstone, and sandstone, greenish-gray, in flat chips up to 1 in. in size; some varicolored chips; gray fine-grained calcareous sandstone.•.•.•.•.. 15 570 Claystone and siltstone, reddish-brown, soft to firm, calcareous; 20 percent greenish-gray chips; some fine-grained sandstone and gypsum; cutting size, variable--large near 670 ft--small near 690 ft; in crease in sand content at 690 ft; slow drilling 693 to 700 ft . 130 700 Sandstone, reddish-brown, mainly very fine to fine grained, calcareous, in grains and chips; calcareous siltstone, some gray claystone, and rare pebbles ••••.•. 10 710 Siltstone and claystone, reddish-brown to gray, cal careous, soft to firm, some fine-grained sandstone, a trace of gypsum, and a few ~-in. pebbles.•••••••.•.•• 60 770 41 Table 9.--Selected logs of we11s--Continued Material Thickness Depth (D-28-7)27cdb-l - Continued Summerville Formation - Continued Siltstone, claystone, and fine- to medium-grained, greenish-gray to red calcareous soft to firm sandstone ..•...... •..•...... •...... •...... 25 795 Curtis Formation Siltstone, claystone, and fine- to medium-grained, greenish-gray to red calcareous sandstone . 15 810 Siltstone and claystone, brown and gray-green, and gray very fine grained sandstone; gypsum at 820 ft; and many large flat chips of green siltstone below 700 ft . 80 890 Entrada Sandstone Siltstone, claystone, and fine- to medium-grained, greenish-gray to red calcareous sandstone; some gypsum at 900 ft; increase in sandstone at 910 ft; flakes of coal (?) at 920 ft . ..•...... 70 960 Sandstone, reddish-brown, very fine to fine-grained, sticky, silty, clayey, calcareous, with chips of red to gray siltstone and claystone . 240 1,200 No record . 25 1,225 Siltstone, claystone and very fine to fine-grained brown and gray to gray-green sandstone; increase in gypsum at 1,400 ft •.•...... •...... •.••.•...... 215 1,440 Sandstone, reddish-brown, fine-grained, silty, clayey, and chips of green-gray claystone; claystone content decreases with depth...... •.....•..•... 50 1,490 Sandstone, reddish-brown, very fine grained, calcareous, silty, with chips of soft to firm reddish-brown to greenish-gray siltstone and claystone, and with medium to coarse gray to white fragments (gypsum?) . 25 1,515 Carmel Formation Sandstone, mostly gray, very fine grained, calcareous, silty, with chips of siltstone and claystone . 55 1,570 Claystone, siltstone, and very fine to fine-grained soft to firm calcareous sandstone, with large flat chips of reddish-brown siltstone••.....•...•.•.••..•..•• 10 1,580 42 Table 9.--Selected logs of wells--Continued Material Thickness Depth (D-28-7)27cdb-~ - Continued Carmel Formation - Continued Claystone, siltstone, and sandstone, gray to reddish- brown " '" . 10 1,590 Claystone, siltstone, and sandstone, greenish-gray, soft, with a trace of gypsum, and 10 percent chips of reddish-brown siltstone . 10 1,600 Claystone, dark grayish-green to bluish-green, soft, slightly calcareous, with a trace of brown siltstone and gypsum...... •...... 20 1,620 Claystone and siltstone, greenish-gray to red, soft, in small to medium-sized chips . 20 1,640 Claystone and siltstone, greenish-gray to red, soft, in large chips . 40 1,680 Claystone and calcareous siltstone, greenish-gray and dark red, in large chips and flakes, with a trace of gypsum . 10 1,690 Claystone, greenish-gray, and dark-red siltstone; cal careous, soft to moderately firm, in small to large chips and flakes; trace of gypsum, including a fibrous gypsum-calcite vein fragment; some angular calcareous chips near 1,710 ft...... •...... 30 1,720 Siltstone, red and green, soft to moderately firm, in medium to large chips and flakes; chips of limestone and gypsum...... •..•...... 30 1,750 Claystone and siltstone, red and green...... ••..•... 50 1,800 Siltstone, dark-red, soft, and dark-red and greenish gray, calcareous, firm; gray limestone; a few gypsum chips; and a trace of anhydrite at 1,820 Et; dark- red siltstone decreased in amount below 1,830 ft . 40 1,840 Limestone, gray, dense, in small chips, and small to large chips of dark-red and grayish-green calcareous siltstone; trace of anhydrite . 10 1,850 Limestone, gray, in small to medium chips; includes brown and green siltstone and gypsum at 1,880 ft and brown and red siltstone at 1,890 ft . 70 1,920 43 Table 9.--Selected logs of wells--Continued Material Thickness Depth (D-28~7)27cdb-~ - Continued Carmel Formation - Continued Limestone, gray, dense, in small chips; contains some bluish-gray calcareous siltstone and numerous gypsum chips •...... •...... •...... 10 1,930 Clay, volcanic; siltstone and limestone; clay is light buff, lean, soft, plastic, cohesive, and contains small green angular chips of devitrified volcanic glass; siltstone is dark bluish-gray, slightly ce- mented with calcite...... •..•...... •...••.••.•... 20 1,950 Siltstone and limestone with volcanic clay; large chips of bluish-green soft and dark-red firm calcareous siltstone; small chips of gray to buff, dense lime- s tone; gypsum and trace of red jasper•.....•.•.....•.•• 14 1,964 Siltstone, light-green, soft, slightly to non-calcareous; some gypsum; some dark-brown earthy, poorly cemented non-calcareous siltstone, and light-gray, slightly porous limestone at 1,971 ft; brief rough drill action and decrease in penetration rate at 1,975 ft . 16 1,980 Limestone, light to dark-gray, dense, in small chips, and reddish-brown weak to firm ferruginous(?) silt stone; the siltstone cuttings color the entire sample dark red . 9 1,989 Navajo Sandstone Sandstone, silty, very fine to fine-grained, with a red silty matrix; includes cavings of siltstone and lime- s tone 3 ••••••••••••••••••••••••••••••••••••••••••••••••• 11 2,000 Sandstone, silty, very fine to fine-grained; includes chips of white to brownish-red medium-grained sand- stone, gypsum, and cavings . 10 2,010 Sandstone, white, slightly calcareous, in well-rounded, frosted grains, and chips of red calcareous sandstone; some chips of dark-gray limestone; sandstone content increases with depth•..•..•.•••.••....•.•.••..•••..••.. 40 2,050 Sandstone, white, slightly calcareous; some chips of green siltstone; siltstone content increases to about 60 percent at 2,070 ft . 30 2,080 Sandstone, silty, dark-red and white, and green silt- s tone ...... •....••...•...... ••.•...... ••..••...... 12 2,092 44 Table 9.--Selected logs of wells--Continued Material Thickness Depth (D-28-7)27cdb-l - Continued Navajo Sandstone - Continued Siltstone and sandstone; sand occurs primarily as individual grains; siltstone may be cavings(?) .•.•...•• 58 2,150 Siltstone, in green and red chips, and white aeolian sandstone with gypsum; Navajo-type material increases slightly at and below 2,170 ft; sand is very fine grained with silt matrix at 2,200 ft; siltstone is green, red, and white at 2,220 ft; traces of gypsum at intervals; some white limestone at 2,310 ft•..•..•.. 191 2,341 No record •...... •.....•.•..•...... •...... 3 2,344 Cored to 2,353 ft Sandstone, pale reddish-brown to buff, very fine to fine-grained, well rounded to subangular, massive, homogeneous, slightly friable; fragments mostly can be powdered by finger pressure; little or no calcite; core fractured along planes that dip 10° to 70°4 .•••••• 9 2,353 lSample log for first 1,600 ft was from well OW-I, which was 107 ft S. 10° W. of well OW-lA, approximately along strike of formation. Well OW-l was abandoned because of drilling complications. Difference in alti tudes of the two holes is 1 ft. 2Formation tops were picked using various combinations of lithology, geophysical logging, and correlation with other wells and test holes in the general area. 3 1n the interval 1,990-2,341 ft, the red and green siltstone, silty sandstone, and limestone are probably cavings from higher in the hole. 4Sumrnary of core log by L. A. Jackson. 45 Table 9.--Selected logs of wells--Continued Material Thickness Depth (D-28-7)36bbb-l - Driller's log by Binning Drilling Co. Alt. 5,100 Soil . 8 8 Tununk Member of the Mancos Shale l Clay, blue...... •...... ••.... 92 100 Cedar Mountain (?) Formation Clay and gravel, black . 58 158 Brushy Basin Shale Member of the Morrison Formation Hardpan, white . 12 170 Clay and gravel, gray ...... •...... ••..•....••• 25 195 Clay and gravel, white •...... •...... •.•••..•....•...•.• 13 208 Hardpan . 4 212 Clay, gray, and loose gravel• .••....••.••.•....••.••••••• 13 225 Clay and gravel, red . 15 240 Clay, gray, hard in spots, and boulders . 15 255 Clay, red . 15 270 Clay, green, and gravel; salt water . 10 280 Clay and silt, variegated, and loose gravel . 20 300 Clay and silt, red, and gravel . 20 320 Hardpan, red . 14 334 Bentonite, white...... •.. 61 395 Hardpan, gray ...... •..•..•..•..•...••...••••.. 5 400 Bentonite, green...... •...... ••...... •.•..•••.... 10 410 Bentonite, red . 25 435 Clay, red, white, and green "ribbon" (varved?) . 20 455 46 Table 9.--Selected logs of wells--Continued Material Thickness Depth (D-28-7)36bbb-l - Continued Clay...... •.•...... •...... •...••••..•... 30 485 Shale, loose, red . 5 490 Clay, red; water seep . 15 505 Bentonite, white . 25 530 Salt Wash Sandstone Member of the Morrison Formation Clay and sand, white . 40 570 Clay and gravel, red . 15 585 Clay, white . 5 590 Sandstone, white . 15 605 Clay and sand, variegated . 23 628 Sandstone . 10 638 Clay, red, and sandstone; 30 gal water per hour••.. 12 650 Sandstone, hard, gray, and clay••...... •....•..•••••••••. 15 665 Clay, red.•...... •...... 5 670 Gypsum ..•.••. 10 680 Conglomerate, very hard . 7 687 Gyp sum, red It •••••••••••••••••••••••••••• 13 700 Conglomerate, red . 10 710 2 Gypsum, white; water at 713 ft •••••• 10 720 Conglomerate, hard, and layers of gypsum••...... ••.•.••. 80 800 IFormation tops picked on basis of driller's descriptions. 2Water under flowing artesian conditions after well was cased to 726 ft; first shut-in pressure was 30 ft above land surface. 47 Table 9.--Selected logs of wells--Continued Material Thickness Depth (D-28-8)29cdc-2. Summary log reported by Stanolind Oil Co. Formation tops picked from electric log. Alt. 4,936. Entrada Sandstone: Sandstone and shale, red••.•.•••••••••. 306 306 Carmel Formation: Limestone, gray, green dolomite, red shale, and white to red sandstone •.••.•..•...... •.. 392 698 Navajo Sandstone: Sandstone, white and red ....•...... •. 970 1,668 Kayenta Formation: Sandstone, red-brown...... •..•...... 134 1,802 Wingate Sandstone: Sandstone, orange-red..•.••••...•....•. 521 2,323 Chinle Formation: Shale and sand, maroon•...•...... •.••• 422 2,745 Moenkopi Formation: Upper Moenkopi: Shale, maroon, silty...••..•••.••....• 608 3,353 Sinbad Limestone Member: Limestone, gray, oolitic••.•. 50 3,403 Lower Moenkopi: Shale, red •.•..•..••.•••••.•••••.•.•.• 79 3,482 Kaibab Limestone: Sandstone, gray, and limestone.•••••..•• 80 3,562 Coconino Sandstone: Sandstone, white to tan••••••.•••••.•• 1,143 4,705 Pennsylvanian rocks, undivided: Dolomite and limestone, gray-buff . 1,625 6,330 Molas Formation: Shale, red-green, and gray limestone•.•.• 220 6,550 Mississippian rocks, undivided: Dolomite, white-tan, and limes tone . 610 7,160 48 Table 9.--Selected logs of wells--Continued Material Thickness Depth (D-28-8) 29dcb-1. Log summarized from field notes by R. J. Madsen, IePA. Alt. 4,896.5 Entrada Sandstone Siltstone and sandstone, brown to dark brown.••...... •. 244 244 Carmel Formation Shale, hard, gray ...... •...... •..•....•..••.• 17 261 Shale, light-brown...... •....•....••..••..•..•••...... 2 263 Shale, gray ...... •..•...... •.•.•••.••....•. 4 267 Shale, brown...... •...... •..•.....•...••••..••. 5 272 Shale, gray . 18 290 Shale, brown . 7 297 Shale, gray . 15 312 Shale, light-brown..••.••..••.•.••.•.••.•..••..•••.•••••• 7 319 Shale, gray . 11 330 Shale, sticky, blue-gray....•..•.•....•.••.•.••..••••.••• 19 349 Shale, brownish-gray ...... •..••...... ••••.••••• 7 356 Shale, blue-gray••.•••....•....•..••••.••...••••...... 5 361 Shale, gray ...... •....•.....••..••..•.••••.•• 11 372 Shale, soft, light-brown...•...••.••.•••.•••.•••••••.•••. 23 395 Shale, soft, light-gray ..••..•.••..•...••••.•••••••..•••. 8 403 Shale, hard, dark-gray . 7 410 Shale, soft, brown . 7 417 Shale, hard, gray . 31 448 Limestone, hard, white . 19 467 Shale, hard, gray . 16 483 Limestone, hard, white, shaly.•.•••••••••...•••.••••..•.. 13 496 Shale, soft, light-brown•...••.•••.•••.•..••.•••••.•..••. 1 497 Shale, red . 18 515 Shale and thin layers of red sandstone . 7 522 Limes tone, tan . 3 525 Shale, brown . 7 532 Shale, dark-brown . 13 545 Limestone and shale, light-brown.•••••••••••••••••••••••• 5 550 Shale, gray . 5 555 Shale, tan...... ••...... ••••.•••••.• 3 558 Shale, gray . 5 563 Well began to flow 70 gal/min with sand at 562 ft Limestone, hard, gray .•.....••••.....•••...... ••••.•...• 12 575 Sand, gray, shaly..•...... •.•...••••.•.•••••• 1 576 Limestone, hard gray; flow increased to 90 gal/min•••.••• 12 588 Limestone, gray, shaly . 4 592 Limestone, hard gray; flow increased to 670 gal/min at 592 ft . 5 597 49 Table 9.--Selected logs of wells--Continued Material Thickness Depth (D-28-8)29bcd-l - Continued Carmel Formation - Continued Limestone, gray; flow increased to 1,350 gal/min at 597 ft . 3 600 Limestone and shale, gray . 5 605 Limes tone, gray . 2 607 Shale, brown . 4 611 Limestone, gray, shaly; difficult drilling . 9 620 Shale, gray, spongy; difficult drilling.•.•...... 8 628 Limestone, gray; flow 1,350 gal/min; logged hole . 1 629 Shale, gray ...... •...... •...... •...... 14 643 Shale, sandy, gray ...... •...•...... 2 645 Shale, blocky, gray; drills into many chips . 5 650 Shale, sandy, brown ...... •... 4 654 Shale, gray ...... •...... 8 662 Shale, sandy, brown...... •...... 1 663 Shale, sandy, gray; flow increased to 1,570 gal/min...•.. 3 666 Shale, loose, brown...... •....•..•...... • 2 668 Navajo Sandstone Sandstone, brown; flow increased to 2,240 gal/min and then reduced to 1,800 gal/min because (?) of caving.... 20 688 Well was cased to 679 ft and sealed by pressure grout ing from both bottom and top. Sandstone, fine, yellow; after drilling out grout, flow resumed at 280 gal/min . 7 695 Sandstone, yellow; flow 311 gal/min...... •...... 47 742 Sandstone, fine, yellow, in alternating hard and soft layers ...... •...... 19 761 Note: Drilling discontinued at 761 ft because loose sand could not be controlled. Depth of hole after test pumping was 727 ft; on September 3, 1975, depth was 722 ft. 50 Table 9.--Selected logs of wells--Continued Material Thickness Depth (D-28-8)33bbb-l. Summarized from sample log by W. G. Hannah and T. P. Condiff, Los Angeles Department of Water and Power. Alt. 4,883.6. Note: Log based on sampling intervals of 10 ft or less. Entrada Formation No record . 10 10 Sandstone, red, very fine to fine-grained; no chips, mostly quartz grains . 10 20 Sandstone, red, very fine to fine-grained . 30 50 Sandstone, reddish-brown, very fine to fine-grained; some gray sandstone; gypsum fibers common . 10 60 Sandstone, reddish-brown, very fine to fine-grained . 10 70 Sandstone, reddish-brown, fine- to medium-grained, with gypsum and jasper . 10 80 Sandstone, brown, fine- to medium-grained .•..•...•. ; ..•.. 10 90 Sandstone, reddish-brown, fine- to medium-grained traces of gypsum and jasper...... •.••..•... 20 110 Sandstone, reddish-brown, very fine to medium-grained .... 10 120 Sandstone, reddish-brown, very fine to medium-grained, 90 percent; 10 percent gray, poorly cemented, very fine grained sandstone, with chips of well-cemented (calcite) fine-grained sandstone, and scattered gray, black, and red angular rock fragments •..•...••.•.•.••.. 10 130 Sandstone, fine- to coarse-grained, with gray calcareous very fine grained silty sandstone chips ...... •.. 10 140 Sandstone, brown, very fine to fine-grained, with clayey siltstone . 10 150 Sandstone, reddis~-brown, very fine to fine-grained, commonly cemented with calcite; reddish clayey silt- stone increasing . 10 160 Sandstone, reddish-brown, very fine to fine-grained, and reddish clayey siltstone with a trace of gypsum.•.. 10 170 51 Table 9.--Selected logs of wells--Continued Material Thickness Depth (C-28-8)33bbb-l - Continued Entrada Formation - Continued Sandstone, reddish-brown, very fine to fine-grained; chips of gray noncalcareous siltstone common . 5 175 Sandstone, reddish-brown, very fine to fine-grained, Clayey, many chips of sandstone cemented with calcite, and many chips of gray clayey siltstone . 10 185 Sandstone, brown, fine to coarse-grained, with sharp angular chips of gray clayey siltstone . 5 190 Sandstone, reddish-brown, very fine to fine-grained with chips of gray clayey siltstone . 10 200 Sandstone, brown, very fine to fine-grained, and chips of gray clayey siltstone . 10 210 Sandstone, reddish-brown, very fine to fine-grained to silty and clayey; gray clayey siltstone chips common •••...•.••..•.•.••••••••••••••••••••••••••••••••• 10 220 Sandstone, silty, clayey, with reddish-brown chips, very fine grains and much clay.••••.••••.•..•••.••.•••• 10 230 Sandstone, reddish-brown to gray, very fine grained to silty and clayey, in chips the size of coarse grains.•• 10 240 Sandstone, reddish-brown to gray, very fine grained, silty, clayey, soft to hard; chips are sticky when wet; trace of rounded white fragments (gypsum?) in bottom 10 ft . 20 260 Sandstone, very fine grained, silty, clayey, in chips; some gypsum and hard gray sandstone . 10 270 Sandstone, brown to gray, very fine grained, silty, clayey, in chips; trace of gypsum.•••...... •.••••••••. 4 274 Carmel Formation Siltstone and claystone, gray calcareous, angular frag ments, very fine to medium sand, and trace of red fine- grained silty sandstone and gypsum . 6 280 Sandstone, gray calcareous, very fine to fine-grained silty, clayey; white gypsum common; trace of red sands tone . 10 290 52 Table 9.--Selected logs of wells--Continued Material Thickness Depth (D-28-8)33bbb-l - Continued Carmel Formation - Continued Sandstone, very fine to medium-grained, siltstone, and hard gray claystone, angular fragments . 10 300 Sandstone, fine to medium-grained, siltstone, and clay stone, light-gray to dark-gray; gypsum fragments and red-brown sandstone chips; probably contains cavings from overlying Entrada Formation . .••.•..••.••.•.•.•.•.• 100 400 Limestone, gypsum, and claystone in very large chips, and fine to medium-grained reddish-brown sandstone..... 30 430 Gypsum and calcareous siltstone and claystone, white to dark-gray; much of claystone is soft•...... •. 10 440 Siltstone and claystone, dark-gray, calcareous, hard to soft, and trace of gypsum...... ••.•...... 10 450 Limestone, siltstone, and fine- to medium-grained sandstone, in large chips, with much clay ...... •....•. 10 460 Limestone, siltstone, and fine- to medium-grained sand- stone, in large chips; much gypsum and some clay . 55 515 Gypsum with siltstone and claystone, dark-gray to red; some slightly calcareous ••..•..•.....•.....•••••..•.•.. 25 540 Siltstone and claystone, dark gray to reddish-brown, slightly calcareous; trace of gypsum....•...... •. 10 550 Limestone, silty, siltstone, and claystone, dark gray. Some is reddish-brown and calcareous with trace of gypsum. Rough drill action in several thin layers between 600 and 610 ft 1 •••••••••••••••••••••••••••••••• 110 660 Limestone, argillaceous, limy siltstone, and clay stone, mostly dark gray; soft to firm chips up to 1/4 in. across; red-brown very soft mudstone (cav- ings?); much gypsum in lower 10 ft. . 20 680 Sandstone, brown-to-tan and gray, fine-grained, cal- careous, with red-brown siltstone and gypsum . 5 685 Sandstone, gray to tan, fine-grained, calcareous; trace of limy siltstone and claystone•...... 5 690 Sandstone, gray to tan; few cutting returns •••.•••••.•... 10 700 53 Table 9.--Selected logs of wells--Continued Material Thickness Depth (D-28-8)33bbb-l - Continued Carmel Formation - Continued Sandstone, very fine grained, siltstone, and clay stone, reddish-brown; 10 percent gray to tan chips of very fine grained calcareous sandstone; chips of white gypsum, gray limy siltstone and claystone cornman; intermittent rough drill action at 698-702 and 708-709 ft '" . 9 709 Navajo Sandstone Clay, soft, light-gray, gypsum, reddish-brown calcar eous sandstone, siltstone, and shale; few cutting returns ...... •...... •.••...... 11 720 Sandstone, light-gray to tan, very fine to fine-grained, moderately calcareous, 65 percent; 35 percent cavings from above 709 ft. Percentage of cavings diminishes with depth, and sandstone is very fine to medium grained below 760 ft . 60 780 Sandstone, white to yellow, 75 percent; 25 percent cav ings; rough drill action l 785-790 ft and 800-803 ft; cuttings highly calcareous 810-815 ft•..•...... 35 815 Sandstone, white, 75 percent; 25 percent cavings . 10 825 Sandstone, mostly yellow; chips well cemented with calcite; 25 percent cavings . 6 831 Cored to 861 ft Core 76UTl. Depth interval 834.7-835.2 ft. Sandstone, light-tan with white spots. Bedding plane present; bedding plane 20°. Well cemented with silica. Subarkose, moderately sorted; laminae of very fine to fine sand interlayered with laminae of fine and medium sand. (See fig. 5.) Moder ate optical orientation of grains with bedding planes. Rounded quartz grains, 80-95 percent; subrounded to rounded, partly weathered feldspar, 5-15 percent. Rounded chert is about the only rock type and is found mostly in the medium sand. Grains well packed with microstyolitic boun daries between some grains. Very little matrix; that present is silica, generally as fibrous chalcedony and sparse clay particles. 2 54 Table 9.--Selected logs of wells--Continued Material Thickness Depth Navajo Sandstone - Continued Sandstone, white to light-tan; ranges from massive to thinly bedded; cross beds range from 1/16 to 2 in. in thickness, some sections appearing laminated with alternate layers of very fine to fine and medium- to coarse-grained sandstone; dip of crossbedding ranges from 10° to 25°; fracture at 841 ft dips 60° and is healed wi t h gypsum 3 ••••••••••••••••••••••••••••••••••• 30 861 Sandstone, yellow-brown, very fine to coarse-grained..... 19 880 Sandstone, light-gray to yellow, very fine to coarse grained, firm but friable; rough drill action 912- 913 ft; cuttings below 920 ft about half chips and half grains; below 990 ft nearly all cuttings reduced to grains, which are obscured by cavings; cavings appear to make up 40-95 percent of cutting returns..... 190 1,070 Sandstone, light-gray to yellow, very fine to coarse grained, mostly in chips; rough drill action i 1,072 1,075 ft; white calcite chips 1,080-1,090 ft with traces below...... ••...... 66 1,136 Cored to 1,158 ft Core 76UT2. Depth interval 1,139.7-1,140.3 ft. Sandstone, light-tan. No bedding plane visible to the eye. Well cemented with silica. Cherty subarkose, well sorted. Subrounded to rounded quartz, 75-90 percent; subrounded feldspar, 5-15 percent; rounded chert, 5-10 percent; few other rock fragments. Grains well packed with microstyolitic boundaries be tween some grains. Less matrix than in samples 76UTl or 76UT3; matrix material mainly fibrous chalcedony, some of which is spherulitic. (See fig. 7.) 2 Sandstone, light-grayish-brown, massive, homogeneous, moderately hard; 60 to 75 percent fine grained; calcite rare; fractures generally dip 10°-15° but 4 as much as 45° •••••••••••••••••••••••••••••••••••••••• 14 1,150 Sandstone, light-grayish-brown; less cemented than interval above; alternately massive and crossbedded with some laminations less than 1/16 in. thick; crossbedding dips range from 10° to 70°; fractures dip 10° to 30°; fracture at 1,156 ft filled with 4 calcite •••••••....•••••••••••••••••••••••••••••••••••• 8 1,158 55 Table 9.--Selected logs of wells--Continued Haterial Thickness Depth O:L~8-8) 33bbb-} - Continued Navajo Sandstone - Continued No record . 2 1,160 Sandstone, light-gray to yellow, very fine to coarse grained, with trace of calcite; about half in chips; amount of cavings decreasing ...... •. 110 1,270 Sandstone, tan and brown, fine-grained, limestone, and white calcite; some reddish-brown sandstone below 1,350 ft; few cutting returns 1,390-1,400 ft . 130 1,400 Sandstone, reddish-brown to tan, very fine to fine grained and friable chips; few cuttings below 1,410 ft . 40 1,440 Sandstone, brown to tan, very fine grained, limestone, and white calcite chips ...... ••...... 25 1,465 Cored to 1,485 ft Core 76UT3. Depth interval 1,476.3-1,476.8 ft. Sandstone, light-tan Crossing dips 28°. Better cemented with silica than the two samples above. Well-sorted subarkose. Subangular to subrounded quartz, 80-95 percent; subangular to subrounded feldspar, 5-15 percent; and rounded chert. Hore opaque minerals, weathering of feldspars, and iron oxide grain coatings than observed in samples above. Packing and grain boundaries as noted above. Hatrix similar to that in sample 76UTl; 1 percent or less of coarsely crystalline carbonate cement. (See fig. 8.)2 Sandstone, light-tan, very fine to fine-grained massive, hard but slightly friable; reddish-brown banding 1/8 in. thick at 1,466 and 1,469 ft; dips steeply (one was 50°); many intersecting fractures, either open (?) for partly to completely healed with calcite, have dips of 50° to 70°; fractures probably cause of rough drill action at about 1,471 ft s .••••••.• 10 1,475 Sandstone, light-tan, very fine to fine-grained, hard but slightly friable; little calcite cement; parts contain hairline to 1/16 in. laminations that dip 10°_25°; fractures dip 25°-35° and 50°-80° and some 4 are partly filled with calcite •• •••••••••••••••••••••• 10 1,485 No record . 5 1,490 56 Table 9.--Selected logs of wells--Continued Material Thickness Depth Navajo Sandstone - Continued Sandstone, brown to tan, very fine grained, limestone and whi te calci te chips . 30 1,520 Sandstone, light brown to tan, very fine grained, limestone and white calcite chips ...... •.... 100 1,620 Kayenta Formation Sandstone, reddish-brown, very fine grained, calcar eous chips with chips from previous interval; chips at 1,640 ft are angular and calcareous . 30 1,650 Sandstone, reddish-brown, very fine to fine-grained, calcareous; chips are flat and angular and are smaller than chips from Navajo; intermittent rough drill action 1,679-1,680 ft ...... •...... 30 1,680 Sandstone, silty, and sandstone; reddish-brown to flesh-colored, very fine grained, angular chips; some soft greenish-gray siltstone and claystone and tan sands tone . 5 1,685 lSuch "rough drilling" commonly is caused by thin hard layers, and this may be the case in the Carmel Formation. But such action also could be due to the drill binding in fractured zones, which is the probable case in the Navajo Sandstone. 2Sample description by U.S. Geological Survey. 3Summary of core log by J. T. Dunlap, Los Angeles Department of Water and Power. 4Summary of core log by L. A. Jackson, Los Angeles, Department of Water and Power. 5Summary of core log by W. G. Hannah. 57 Table IO.--Selected chemical analyses of water samples Location: See text for description of well- and spring-numbering system. Geologic unit: 200MSZC, rocks of Mesozoic age, undivided; 220NVJO, Navajo Sandstone; 22lCRML, Carmel Formation; 22ISLWS, Salt Wash Sandstone Member of Morrison Formation. Discharge: E, estimated. Agency making analysis: GS, U.S. Geological Survey; LA, Los Angeles Department of Water and Power; UR, Utah Department of Health. I I II w .... w ""~ .. o~ w ~ ~ Q -::; .... 00 .... ';;;' ~ ~ 0 u ~ ~ .c 8 ~ " ~ ~ " ~ 00 .- 00 u ';;;' u> .... w " >, " ~ ~ w u " 8 z ~E ~ "~ '" -; ~ w w '" "'"0 ;; .... ? 9 9 ~ 0 .... 8 ...... -;;; w .c "~ "" "3~ ~ ~ ~ .. u . " ~ 00 .... .- 8 8 .. " 0 " .. ~ .... OD ~ " u ~ '" w ~ 00 u ".-~ " 0 "00.. Location I 8 U " '" ~ ~ w 0 0 .... ~ .-u ~ ° -;;; 0 0 ~ 8 0 .... .c ~"' " ~ " "" ~ .... 0 OD ...... ~ ::... 0 .... OD .- .., is ...." .... ~ -5 '" "" .. ~ "N~ ~ .. ~ 0 o u w .... "'~ OD 0 0 u .c ...... ~ o .., ~ .... ~'" "00 0- W ° ~ U ~~ o~ .0 U .... 0""< 0""< W 8 '"u 8 ~ .. '" ~ ..,~ .o~ ~ .- " "" Z " u " .. ~ w ~ w ~ ~ " " "" '" 0 .... 0 .... W W <1l ~ W W "<1l "<1l '"'OIl "<1l "w~ 0 u 8 8 " u OD .. " " 00 .... U " .. " " .0 .... ~ ", " ", ", ", 0 ", , , " ~ ~~ ~~ ....8~ ~ ~ ~B " ' >, ~ ~ " " ~ ~ ~ ~ ~~ " .... ""~ ""0 OD .. ," ,'" ...... 0 '" ...... "~ "~ .... 0 .. 0,", u 0 ~ ~ '" 0,", ~~ 0,", 0,", 0,", 0,", 0,", 0,", 0 .c .c .c'" 0'"' o '" ~ u~ m~ .o~ o"w~"'"' "~'"' ...... <1l .. W U "~ "~ "~ "'~ "~ "~ ~ ._" ~0< "~ "''"' ~-g ~OD ._ a " w 0 0...... "8 ;JJ be ~~ " '"' 00 OD " .., "0 " OD .. "'.., .~ " OD " OIl .~ .~W " OD ',.-1 .,.-1 .,.., ;J. .,.., '" - .z '"'" '" .... '" .... '" " "'~ "'~ "'~ '" " '" " '"'" (D- 28- 7) 11cdb-S1 7-17-75 221SLWS - 230 51 430 7.3 278 1,300 71 1.6 0.03 530 2,250 780 560 2,960 GS 27cdb-1 11-20-75 220NVJO 1,990 2,353 )OOE 16.0 20 130 48 21 4.2 279 0 320 9.7 .2 0.00 .00 - 683 520 290 973 7.4 GS IJJ 36bbb-1 7-17-75 221SLWS 726 800 1.8 14.5 40 11 4.1 450 1.7 174 0 770 54 1.1 .01 .00 250 1,390 44 0 2,050 8.0 GS (Xl (D-28-8) 29cdc-1 6-16-71 220NVJO 720 764 10 0 126 50 520 5.1 291 2 618 463 .4 340 1,940 520 280 3,000 8.2 UIl 8-28-75 55 17.0 1,800 140 37 460 4.2 300 0 640 460 .4 .01 .03 250 1,900 500 260 2,700 7.1 GS 29dcb-1 11- 26-73 221CRML 560 597 1,350 -- 700 240 460 6.3 121 0 2,000 1,100 .8 .04 .18 470 4,580 2,700 2,600 5,460 7.3 GS 1-22-74 220NVJO 679 695 280 - 420 120 510 6.3 191 0 1,300 860 .6 .12 .03 480 3,350 1,500 1,400 4,440 7.5 GS 2- 9-74 679 761 3,110 - 300 96 480 6.2 231 0 1,000 680 .7 .03 .09 350 2,690 1,100 960 3,920 7.4 GS 33bbb-1 8-21-75 220NVJO 704 1,250 500E 17.5 630 94 71 780 3.9 286 0 690 850 .8 .02 .00 520 2,640 530 290 4,000 7.3 GS 11-24-75 2,800 17.5 95 28 760 3.7 289 0 660 800 .7 .01 .00 530 2,500 350 120 4,050 7.0 GS 12-29-75 2,800 17.5 650 78 26 840 3.9 187 0 620 890 .8 .00 .03 550 2,560 300 150 4,380 7.1 GS 33cdd-1W 7-14-75 200MSZCl ? 2,425 72 27 2,100 5.0 - 362 3,060 .3 130 7,210 290 9,800 8.0 LA 33cdd-1S2 8- 6- 75 200MSZC 3 611 1,296 180 18.0 1,500 140 63 140 7.0 229 0 470 190 .2 .02 .00 70 1,140 610 420 1,750 7.4 GS 8- 8-75 221CRML 611 621 <1 18.0 140 480 130 360 12 57 0 1,100 890 .3 .08 .00 260 3,010 1,700 1,700 4,200 8.1 GS 8-11-75 221CRML 663 673 136 62 136 5.0 - 456 166 .2 50 1,260 595 1,650 7.3 LA 8- 8-75 220NVJO 756 766 35 17.5 1,800 140 63 91 5.1 226 0 430 110 .2 .02 .00 80 964 610 420 1,490 7.1 GS 8- 7-75 220NVJO 901 911 26 17.0 1,400 98 53 78 5.4 232 0 310 68 .2 .00 .00 30 740 460 270 1,160 7.1 GS 8- 7-75 220NVJO 1,051 1,061 22 17.5 1,200 98 51 110 6.3 226 0 350 88 .2 .10 .00 30 827 450 270 1,300 7.3 GS 8- 7-75 220NVJO 1,286 1,296 21 17.5 1,300 80 39 300 6.7 279 - 180 410 .3 .01 .00 60 1,170 360 130 2,100 GS 8-21-75 220NVJO 756' 1,296 200E 17.5 2,700 110 52 130 5.6 225 0 380 130 .2 .01 .00 60 933 490 310 1,400 7.0 GS 1Sample probably included water from Carmel (?) to Chinle Formations. 2Samples from this well include drill-stem tests of IO-foot zones between a straddle packer. 3 Sampled while perforations in Carmel and Navajo Formations were open to hole. 4Samp l ed from flow after zones above 756 feet were squeeze-cemented and additional perforations made between the original four IO-foot zones. Table 11.--Measurements of discharge, temperature, and specific conductance of water from wells Location: See text for description of well- and spring-nwnbering system. Geologic unit: 200MSZC, rocks of Mesozoic age, undivided; 220NVJO, Navajo Sandstone; 221CRML, Carmel Formation; 221SLWS, Salt Wash Sandstone Member of the Morrison Formation; 310KIBB, Kaibab Limestone. Discharge: E, estimated. Agency making analysis: GS, u.s. Geological Survey; LA, Los Ange1e" Department of Water and Power; illl, Utah Department of Health. Depth to Depth to Specific Date top of bottom of Geo logic Discharge Temper- conductance Agency Location of Time sample sample unit (gal/min) ature (~mho/cm making sample interval interval (OC) at 25°C) analysis (ft) (ft) (D- 28-7) 27cdb-1 11-20-75 0020 1,990 2,353 220NV.IO 300E 16.0 973 GS 11- 20-75 0110 300E 988 LA 10- 6-76 1600 10 15.6 2,500 GS 36bbb-1 7-17-75 1015 726 800 221SLWS 1.8 14.5 2,050 GS 8-21-75 1525 1.9 15.5 2,080 GS 11-15-75 1530 2.0 14.0 2,100 GS 3-16-76 1812 2.0 13.5 2,180 GS 4-14-77 1302 2.0 14.0 2,050 GS (D- 28-8) 29cdc-1 6-16-71 720 764 220NV.JO 10 3,000 illl 8-15-74 21.0 2,990 LA 7-17-75 48 17.0 GS 8- 7-75 1533 60 17.0 3,000 GS 8-21-75 1105 60 17.0 3,000 GS 8-28-75 1320 55 17.0 2,700 GS 9- 4-75 1610 17.0 2,900 GS 11-15-75 1137 1.5 16.5 2,900 GS 7-22-76 0950 5.0 17.0 2,650 GS 3-31-77 1720 47 17.0 2,450 GS 6-15-77 0940 80 17.0 2,550 GS 29dcb-1 11-19-73 560 564 221CRMJ 30E 7,000 GS 11-22-73 560 580 90 5,000 GS 11- 24-73 560 592 670 4,000 GS 11- 26-73 560 597 1,350E 5,460 GS 12- 1-73 560 610 1,350 5,000 GS 12- 6-73 560 628 1,350 5,100 GS 1- 5-74 560 662 1,520 GS 1- 6-74 560 668 200MSZC 1 1,570 4,900 GS 1 1- 7-74 560 675 200MSZC 2,240 GS 1-22-74 679 695 220NV .IO 280 4,440 GS 1-23-74 679 742 311 GS 2- 8-74 0840 679 761 1,470 3,750 GS 2- 9-74 1130 3,110 3,920 GS 4-13-74 3,910 LA 10- 4-74 24.0 4,200 LA 10-30-74 23.0 3,880 LA 7-17-75 400E 16.5 4,000 GS 11-15-75 1150 1.0E 15.0 5,600 GS 33bbb-1 8-19-75 1400 700 1,250 220NV.IO 4,000 LA 8-19-75 1401 4,000 GS 8-20-75 4,250 LA 8-21-75 1015 500E 17.5 4,000 GS 8-22-75 500E 4,950 LA 8-30-75 500E 4,400 LA 9- 1-75 500E 4,400 LA 9- 4-75 500E 4,200 LA 9- 22-75 770 4,060 LA 9- 26-75 1800 1,600 4,100 LA 9- 29-75 1815 2,150 4,170 LA 11-17-75 HOO 1.0E 3,450 GS 11-24-75 1025 2,800 17 .5 4,050 GS 11- 24-75 1026 17 .5 4,370 LA 11-26-75 2045 17.0 4,000 GS 11-27-75 0255 17 .5 4,450 GS 11-27-75 0700 17.0 4,410 LA 11-27-75 1100 17.5 4,420 LA 11-27-75 1730 17.5 4,400 LA 59 Table ll.--Measurements of discharge, temperature, and specific conductance of water from wells--Continued Depth to Depth to Specific Date top of bottom of Geologic Discharge Temper- conductance Agency Location of Time sample sample unit (gal/min) ature (~mho/cm making sample interval interval ("C) at 25"C) analysis (ft) (ft) (D-28-8)33bbb-1 11-27-75 2005 700 1,250 220NVJO 2,800 17 .5 4,450 GS Continued 11-28-75 1500 17 .5 4,350 LA 11-30-75 1555 17.5 4,420 GS 12- 1-75 1500 17.5 4,360 LA 12- 3-75 2100 17 .5 4,340 LA 12- 5-75 1010 17 .5 4,400 GS 12- 6-75 2100 17.5 4,100 LA 12- 9-75 1240 17.0 4,300 LA 12-12-75 0300 17 .5 4,320 LA 12-15-75 0945 4,330 LA 12- 20-75 2300 4,320 LA 12-23-75 2100 4,320 LA 12-29-75 0910 17 .5 4,380 GS 12- 29-75 0915 17 .5 4,380 LA 6-15-77 1015 50E 18.0 3,600 GS 33cdd-1W 5- 24-75 3,493 3,530 310KIBB 5,000 (2) 5- 24-75 1201 3,595 3,700 ( 3) 2,700 LA 7-14-75 1730 1,350 2,425 200MSZC4 9,800 LA 7-14-75 1750 1,350 2,425 9,800 LA 33cdd-1SS 7-21-75 1030 794 795 220NV JO 34 17.5 GS 8- 5-75 1915 611 1,296 200MSZCl 180 18.0 1,750 GS 8- 6-75 2355 611 1,061 171 17 .5 1,550 LA 8- 7-75 0050 1,286 1,296 220NVJO 21 17.5 2,100 GS 8- 7-75 0051 1,286 1,296 2,000 LA 8- 7-75 0052 1,286 1,296 2,100 LA 8- 7-75 1418 611 911 200MSZC l 120 17.5 1,450 LA 8- 7-75 1422 1,051 1,061 220NVJO 22 17 .5 1,300 GS 8- 7-75 1423 1,051 1,061 1,000 LA 8- 7-75 1424 1,051 1,061 1,250 LA 8- 7-75 2311 901 911 26 17.0 1,160 GS 8- 7-75 2312 901 911 1,150 LA 8- 7-75 2313 611 766 200MSZC 1 100 17.0 1,490 GS 8- 8-75 0140 756 766 220NVJO 35 17.5 1,490 GS 8- 8-75 0141 756 766 1,500 LA 8- 8-75 1724 611 621 221CRML 4,250 LA 8- 8-75 1725 611 621 <1.0 18.0 4,200 GS 8- 8-75 1726 611 621 5,720 LA 8-11-75 220NVJO 1,700 LA 8-11-75 1159 663 673 221CRML 1,550 LA 8-11-75 1201 663 673 1,650 LA 8-13-75 1400 756 1,2966 220NVJO 1,450 LA 8-13-75 1401 1,490 GS 8-21-75 0937 200E 17.5 1,400 GS 11-15-75 1040 1.5 15.5 1,370 GS 1Included water from Cannel Formation and Navajo Sandstone. 2Field measurement reported by Colt Oil Co. 3S amp 1e probably included water from Carme1(?) Formation to White Rim Sandstone Member of Cutler Formation. 4rnc1uded water from Carme1(?) to Chinle Formations. SSamples from this well include drill-stem tests of IO-foot zones between a straddle packer and composi.te flow from perforations above the packer. 6Samp l ed from flow after zones above 756 feet were squeeze-cemented and additional perforations made between the original four IO-foot zones. 60 PUBLICATIONS OF THE UTAH DEPARTMENT OF NATURAL RESOURCES, DIVISION OF WATER RIGHTS (*)-Out of Print TECHNICAL PUBLICATIONS *No. 1. Underground leakage from artesian wells in the Flowell area, near Fillmore, Utah, by Penn Livingston and G. B. Maxey, U. S. Geo logical Survey, 1944. No. 2. The Ogden Valley artesian reservoir, Weber County, Utah, by H. E. Thomas, U.S. Geological Survey, 1945. *No. 3. Ground water in Pavant Valley, Millard County, Utah, by P. E. Dennis, G. B. Maxey and H. E. Thomas, U.S. Geological Survey, 1946. *No. l~ . Ground water in Tooele Valley, Tooele County, Utah, by H. E. Thomas, U. S. Geological Survey, in Utah State Eng. 25th Bienn. Rept., p. 91-238, pIs. 1-6, 1946. ~ *No. -) . Ground water in the East Shore area, Utah: Part I, Bountiful District, Davis County, Utah, by H. E. Thomas and W. B. Nelson, U.S. Geological Survey, in Utah State Eng. 26th Bienn. Rept., p. 53-206, pIs. 1-2, 1948. *No. 6. Ground water in the Escalante Valley, Beaver, Iron, and Washington Counties, Utah, by P. F. Fix, W. B. Nelson, B. E. Lofgren, and R. G. Butler, U.S. Geological Survey, in Utah State Eng. 27th Bienn. Rept., p. 107-210, pIs. 1-10, 1950. rr No. I· Status of development of selected ground-water basins in Utah, by H. E. Thomas, W. B. Nelson, B. E. Lofgren, and R. G. Butler, U.S. Geological Survey, 1952. *No. B. Consumptive use of water and irrigation requirements of crops in Utah, by C. O. Roskelly and W. D. Criddle, 1952. No. B. (Revised) Consumptive use and water requirements for Utah, by W. D. Criddle, Karl Harris, and L. S. Willardson, 1962. No.9. Progress report on selected ground water basins in Utah, by H. A. Waite, W. B. Nelson, and others, U.S. Geological Survey, 1954. *No. 10. A compilation of chemical quality data for ground and surface waters in Utah, by J. G. Connor, C. G. Mitchell, and others, U.S. Geological Survey, 1958. *No. 11. Ground water in northern Utah Valley, Utah: A progress report for the period 1948-63, by R. M. Cordova and Seymour Subitzky, U.S. Geological Survey, 1965. 61 *No. 12. Reevaluation of the ground-water resources of Tooele Valley, Utah, by J. S. Gates, U.S. Geological Survey, 1965. *No. 13. Ground-water resources of selected basins in southwestern Utah, by G. W. Sandberg, U.S. Geological Survey, 1966. *No. 14. Water-resources appraisal of the Snake Valley area, Utah and Nevada, by J. W. Hood and F. E. Rush, U.S. Geological Survey, 1966. *No. 15. Water from bedrock in the Colorado Plateau of Utah, by R. D. Feltis, U.S. Geological Survey, 1966. *No. 16. Ground-water conditions in Cedar Valley, Utah County, Utah, by R. D. Feltis, U.S. Geological Survey, 1967. *No. 17 . Ground-water resources of northern Juab Valley, Utah, by L. J. Bjorklund, U.S. Geological Survey, 1968. No. 18. Hydrologic reconnaissance of Skull Valley, Tooele County, Utah, by J. W. Hood and K. M. Waddell, U.S. Geological Survey, 1968. No. 19. An appraisal of the quality of surface water in the Sevier Lake basin, Utah, by D. C. Hahl and J. C. Mundorff, U.S. Geological Survey, 1968. No. 20. Extensions of streamflow records in Utah, by J. K. Reid, L. E. Carroon, and G. E. Pyper, U.S. Geological Survey, 1969. No. 21. Summary of maximum discharges in Utah streams, by G. L. Whitaker, U.S. Geological Survey, 1969. No. 22. Reconnaissance of the ground-water resources of the upper Fremont River valley, Wayne County, Utah, by L. J. Bjorklund, U.S. Geological Survey, 1969. No. 23. Hydrologic reconnaissance of Rush Valley, Tooele County, Utah, by J. W. Hood, Don Price, and K. M. Waddell, U.S. Geological Survey, 1969. No. 24. Hydrologic reconnaissance of Deep Creek valley, Tooele and Juab Counties, Utah, and Elko and White Pine Counties, Nevada, by J. W. Hood and K. M. Waddell, U.S. Geological Survey, 1969. No. 25. Hydrologic reconnaissance of Curlew Valley, Utah and Idaho, by E. L. BoIke and Don Price, U.S. Geological Survey, 1969. No. 26. Hydrologic reconnaissance of the Sink Valley area, Tooele and Box Elder Counties, Utah, by Don Price and E. L. BoIke, U.S. Geological Survey, 1969. No. 27. Water resources of the Heber-Kamas-Park City area, north-central Utah, by C. H. Baker, Jr., U.S. Geological Survey, 1970. 62 No. 28. Ground-water conditions in southern Utah Valley and Goshen Valley, Utah, by R. M. Cordova, U.S. Geological Survey, 1970. No. 29. Hydrologic reconnaissance of Grouse Creek valley, Box Elder County, Utah, by J. W. Hood and Don Price, U.S. Geological Survey, 1970. No. 30. Hydrologic reconnaissance of the Park Valley area, Box Elder County, Utah, by J. W. Hood, U.S. Geological Survey, 1971. No. 31. Water resources of Salt Lake County, Utah, by A. G. Hely, R. W. Mower, and C. A. Harr, U.S. Geological Survey, 1971. No. 32. Geology and water resources of the Spanish Valley area, Grand and San Juan Counties, Utah, by C. T. Sumsion, U.S. Geological Survey, 1971. No. 33. Hydrologic reconnaissance of Hansel Valley and northern Rozel Flat, Box Elder County, Utah, by J. W. Hood, U.S. Geological Survey, 1971. No. 34. Summary of water resources of Salt Lake County, Utah, by A. G. Hely, R. W. Mower, and C. A. Harr, U.S. Geological Survey, 1971. No. 35. Ground-water conditions in the East Shore area, Box Elder, Davis, and Weber Counties, Utah, 1960-69, by E. L. BoIke and K. M. Waddell, U.S. Geological Survey, 1972. No. 36. Ground-water resources of Cache Valley, Utah and Idaho, by L. J. Bjorklund and L. J. McGreevy, U.S. Geological Survey, 1971. No. 37. Hydrologic reconnaissance of the Blue Creek Valley area, Box Elder County, Utah, by E. L. BoIke and Don Price, U.S. Geological Survey, 1972. No. 38. Hydrologic reconnaissance of the Promontory Mountains area, Box Elder County, Utah, by J. W. Hood, U.S. Geological Survey, 1972. No. 39. Reconnaissance of chemical quality of surface water and fluvial sediment in the Price River Basin, Utah, by J. C. Mundorff, U.S. Geological Survey, 1972. No. 40. Ground-water conditions in the central Virgin River basin, Utah, by R. M. Cordova, G. W. Sandberg, and Wilson McConkie, U.S. Geo logical Survey, 1972. No. 41. Hydrologic reconnaissance of Pilot Valley, Utah and Nevada, by J. C. Stephens and J. W. Hood, U.S. Geological Survey, 1973. No. 42. Hydrologic reconnaissance of the northern Great Salt Lake Desert and summary hydrologic reconnaissance of northwestern Utah, by J. C. Stephens, U.S. Geological Survey, 1973. 63 No. 43. Water resources of the Milford area, Utah, with emphasis on ground water, by R. W. Mower and R. M. Cordova, U.S. Geological Survey, 1974. No. 44. Ground-water resources of the lower Bear River drainage basin, Box Elder County, Utah, by L. J. Bjorklund and L. J. McGreevy, U. S. Geological Survey, 1974. No. 45. Water resources of the Curlew Valley drainage basin, Utah and Idaho, by C. H. Baker, Jr., U.S. Geological Survey, 1974. No. 46. Water-quality reconnaissance of surface inflow to Utah Lake, by J. C. Mundorff, U.S. Geological Survey, 1974. No. 47. Hydrologic reconnaissance of the Wah Wah Valley drainage basin, Millard and Beaver Counties, Utah, by J. C. Stephens, U.S. Geological Survey, 1974. No. 48. Estimating mean streamflow in the Duchesne River basin, Utah, by R. W. Cruff, U.S. Geological Survey, 1974. No. 49. Hydrologic reconnaissance of the southern Uinta Basin, Utah and Colorado, by Don Price and L. L. Miller, U.S. Geological Survey, 1975. No. 50. Seepage study of the Rocky Point Canal and the Grey Mountain Pleasant Valley Canal systems, Duchesne County, Utah, by R. W. Cruff and J. W. Hood, U.S. Geological Survey, 1976. No. 51. Hydrologic reconnaissance of the Pine Valley drainage basin, Millard, Beaver, and Iron Counties, Utah, by J. C. Stephens, U.S. Geological Survey, 1976. No. 52. Seepage study of canals in Beaver Valley, Beaver County, Utah, by R. W. Cruff and R. W. Mower, U.S. Geological Survey, 1976. No. 53. Characteristics of aquifers in the northern Uinta Basin area, Utah and Colorado, by J. W. Hood, U.S. Geological Survey, 1976. No. 54. Hydrologic evaluation of Ashley Valley, northern Uinta Basin area, Utah, by J. W. Hood, U.S. Geological Survey, 1977. No. 55. Reconnaissance of water quality in the Duchesne River basin and some adjacent drainage areas, Utah, by J. C. Mundorff, U.S. Geological Survey, 1977. No. 56. Hydrologic reconnaissance of the Tule Valley drainage basin, Juab and Millard Counties, Utah, by J. C. Stephens, U.S. Geological Survey, 1977. No. 57. Hydrologic evaluation of the upper Duchesne River valley, northern Uinta Basin area, Utah, by J. W. Hood, U. S. Geological Survey, 1977. 64 No. 58. Seepage study of the Sevier Valley-Piute Canal, Sevier County, Utah, by R. W. Cruff, U.S. Geological Survey, 1977. No. 59. Hydrologic reconnaissance of the Dugway Valley-Government Creek area, west-central Utah, by J. C. Stephens and C. T. Sumsion, U.S. Geological Survey, 1978. No. 60. Ground-water resources of the Parowan-Cedar City drainage basin, Iron County, Utah, by L. J. Bjorklund, C. T. Sumsion, and G. W. Sandberg, U.S. Geological Survey, 1978. No. 61. Ground-water conditions in the Navajo Sandstone in the central Virgin River basin, Utah, by R. M. Cordova, U.S. Geological Survey, 1978. No. 62. Water resources of the northern Uinta Basin area, Utah and Colorado, with special emphasis on ground-water supply, by J. W. Hood and F. K. Fields, U.S. Geological Survey, 1978. No. 63. Hydrology of the Beaver Valley area, Beaver County, Utah with emphasis on ground water, by R. W. Mower, U.S. Geological Survey, 1978. No. 64. Hydrologic reconnaissance of the Fish Springs Flat area, Tooele, Juab, and Millard Counties, Utah, by E. L. BoIke and C. T. Sumsion, U.S. Geological Survey, 1978. No. 65 Reconnaissance of chemical quality of surface water and fluvial sediment in the Dirty Devil River basin, Utah, by James C. Mundorff, 1978. WATER CIRCULARS No. 1. Ground water in the Jordan Valley, Salt Lake County, Utah, by Ted Arnow, U.S. Geological Survey, 1965. No. 2. Ground water in Tooele Valley, Utah, by J. S. Gates and O. A. Keller, U.S. Geological Survey, 1970. BASIC-DATA REPORTS *No. 1. Records and water-level measurements of selected wells and chemical analyses of ground water, East Shore area, Davis, Weber, and Box Elder Counties, Utah, by R. E. Smith, U.S. Geological Survey, 1961. No. 2. Records of selected wells and springs, selected drillers' logs of wells, and chemical analyses of ground and surface waters, northern Utah Valley, Utah County, Utah, by Seymour Subitzky, U.S. Geological Survey, 1962. 65 No.3. Ground-water data, central Sevier Valley, parts of Sanpete, Sevier, and Piute Counties, Utah, by C. H. Carpenter and R. A. Young, U.S. Geological Survey, 1963. *No. 4. Selected hydrologic data, Jordan Valley, Salt Lake County, Utah, by I. W. Marine and Don Price, U.S. Geological Survey, 1963. *No. 5. Selected hydrologic data, Pavant Valley, Millard County, Utah, by R. W. Mower, U.S. Geological Survey, 1963. *No. 6. Ground-water data, parts of Washington, Iron, Beaver, and Millard Counties, Utah, by G. W. Sandberg, U.S. Geological Survey, 1963. No.7. Selected hydrologic data, Tooele Valley, Tooele County, Utah, by J. S. Gates, U.S. Geological Survey, 1963. No.8. Selected hydrologic data, upper Sevier River basin, Utah, by C. H. Carpenter, G. B. Robinson, Jr., and L. J. Bjorklund, U.S. Geo logical Survey, 1964. *No. 9. Ground-water data, Sevier Desert, Utah, by R. W. Mower and R. D. Feltis, U.S. Geological Survey, 1964. No. 10. Quality of surface water in the Sevier Lake basin, Utah, by D. C. Hahl and R. E. Cabell, U.S. Geological Survey, 1965. *No. 11. Hydrologic and climatologic data, collected through 1964, Salt Lake County, Utah, by W. V. Iorns, R. W. Mower, and C. A. Horr, U.S. Geological Survey, 1966. No. 12. Hydrologic and climatologic data, 1965, S~lt Lake County, Utah, by W. V. Iorns, R. W. Mower, and C. A. Horr, U.S. Geological Survey, 1966. No. 13. Hydrologic and climatologic data, 1966, Salt Lake County, Utah, by A. G. Hely, R. W. Mower, and C. A. Horr, U.S. Geological Survey, 1967. No. 14. Selected hydrologic data, San Pitch River drainage basin, Utah, by G. B. Robinson, Jr., U.S. Geological Survey, 1968. No. 15. Hydrologic and climatologic data, 1967, Salt Lake County, Utah, by A. G. Hely, R. W. Mower, and C. A. Herr, U.S. Geological Survey, 1968. No. 16. Selected hydrologic data, southern Utah and Goshen Valleys, Utah, by R. M. Cordova, U.S. Geological Survey, 1969. No. 17. Hydrologic and climatologic data, 1968, Salt Lake County, Utah, by A. G. Hely, R. W. Mower, and C. A. Herr, U.S. Geological Survey, 1969. No. 18. Quality of surface water in the Bear River basin, Utah, Wyoming, and Idaho, by K. M. Waddell, U.S. Geological Survey, 1970. 66 No. 19. Daily water-temperature records for Utah streams, 1944-68, by G. L. Whitaker, U.S. Geological Survey, 1970. No. 20 Water-quality data for the Flaming Gorge area, Utah and Wyoming, by R. J. Madison, U.S. Geological Survey, 1970. No. 21. Selected hydrologic data, Cache Valley, Utah and Idaho, by L. J. McGreevy and L. J. Bjorklund, U.S. Geological Survey, 1970. No. 22. Periodic water- and air-temperature records for Utah streams, 1966-70, by G. L. Whitaker, U.S. Geological Survey, 1971. No. 23. Selected hydrologic data, lower Bear River drainage basin, Box Elder County, Utah, by L. J. Bjorklund and L. J. McGreevy, U. S. Geological Survey, 1973. No. 24. Water-quality data for the Flaming Gorge Reservoir area, Utah and Wyoming, 1969-72, by E. L. BoIke and K. M. Waddell, U.S. Geologi cal Survey, 1972. No. 25. Streamflow characteristics in northeastern Utah and adjacent areas, by F. K. Fields, U.S. Geological Survey, 1975. No. 26. Selected Hydrologic data, Uinta Basin area, Utah and Colorado, by J. W. Hood, J. C. Mundorff, and Don Price, U.S. Geological Survey, 1976. No. 27. Chemical and physical data for the Flaming Gorge Reservoir area, Utah and Wyoming, by E. L. BoIke, U.S. Geological Survey, 1976. No. 28. Selected hydrologic data, Parowan Valley and Cedar City Valley drainage basins, Iron County, Utah, by L. J. Bjorklund, C. T. Sumsion, and G. W. Sandberg, U.S. Geological Survey, 1977. No. 29. Climatologic and hydrologic data, southeastern Uinta Basin, Utah and Colorado, water years 1975 and 1976, by L. C. Conroy and F. K. Fields, U.S. Geological Survey, 1977. No. 30. Selected ground-water data, Bonneville Salt Flats and Pilot Valley, western Utah, by. G. C. Lines, U.S. Geological Survey, 1977. No. 31. Selected hydrologic data, Wasatch Plateau-Book Cliffs coal-fields area, Utah, by K. M. Waddell and others, U.S. Geological Survey, 1978. INFORMATION BULLETINS *No. 1. Plan of work for the Sevier River Basin (Sec. 6, P. L. 566), U.S. Department of Agriculture, 1960. *No. 2 Water production from oil wells in Utah, by Jerry Tuttle, Utah State Engineer's Office, 1960. 67 *No. 3. Ground-water areas and well logs, central Sevier Valley, Utah, by R. A. Young, U.S. Geological Survey, 1960. *No. 4. Ground-water investigations in Utah in 1960 and reports published by the U.S. Geological Surveyor the Utah State Engineer prior to 1960, by H. D. Goode, U.S. Geological Survey, 1960. *No. 5. Developing ground water in the central Sevier Valley, Utah, by R. A. Young and C. H. Carpenter, U.S. Geological Survey, 1961. *No. 6. Work outline and report outline for Sevier River basin survey, (Sec. 6, P. L. 566), U.S. Department of Agriculture, 1961. *No. 7. Relation of the deep and shallow artesian aquifers near Lynndyl, Utah, by R. W. Mower, U.S. Geological Survey, 1961. *No. 8. Projected 1975 municipal water-use requirements, Davis County, Utah, by Utah State Engineer's Office, 1962. No. 9. Projected 1975 municipal water-use requirements, Weber County, Utah, by Utah State Engineer's Office, 1962. *No. 10. Effects on the shallow artesian aquifer of withdrawing water from the deep artesian aquifer near Sugarville, Millard County, Utah, by R. W. Mower, U.S. Geological Survey, 1963. *No. 11 . Amendments to plan of work and work outline for the Sevier River basin (Sec. 6, P. L. 566), U.S. Department of Agriculture, 1964. *No. 12. Test drilling in the upper Sevier River drainage basin, Garfield and Piute Counties, Utah, by R. D. Feltis and G. B. Robinson, Jr., U.S. Geological Survey, 1963. *No. 13. Water requirements of lower Jordan River, Utah, by Karl Harris, Irrigation Engineer, Agricultural Research Service, Phoenix, Arizona, prepared under informal cooperation approved by Mr. W. W. Donnan, Chief, Southwest Branch (Riverside, California) Soil and Water Conservation Research Division, Agricultural Research Service, U.S.D.A., and by W. D. Criddle, State Engineer, State of Utah, Salt Lake City, Utah, 1964. *No. 14. Consumptive use of water by native vegetation and irrigated crops in the Virgin River area of Utah, by W. D. Criddle, J. M. Bagley, R. K. Higginson, and D. W. Hendricks, through cooperation of Utah Agricultural Experiment Station, Agricultural Research Service, Soil and Water Conservation Branch, Western Soil and Water Management Section, Utah Water and Power Board, and Utah State Engineer, Salt Lake City, Utah, 1964. *No. 15. Ground-water conditions and related water-administration problems in Cedar City Valley, Iron County, Utah, February, 1966, by J. A. Barnett and F. T. Mayo, Utah State Engineer's Office. *No. 16. Summary of water well drilling activities in Utah, 1960 through 1965, compiled by Utah State Engineer's Office, 1966. 68 *No. 17. Bibliography of U.S. Geological Survey water-resources reports for Utah, compiled by O. A. Keller, U.S. Geological Survey, 1966. *No. 18. The effect of pumping large-discharge wells on the ground-water reservoir in southern Utah Valley, Utah County, Utah, by R. M. Cordova and R. W. Mower, U.S. Geological Survey, 1967. No. 19. Ground-water hydrology of southern Cache Valley, Utah, by L. P. Beer, 1967. *No. 20. Fluvial sediment in Utah, 1905-65, A data compilation by J. C. Mundorff, U.S. Geological Survey, 1968. *No. 21. Hydrogeology of the eastern portion of the south slopes of the Uinta Mountains, Utah, by L. G. Moore and D. A. Barker, U.S. Bureau of Reclamation, and J. D. Maxwell and B. L. Bridges, Soil Conservation Service, 1971. *No. 22. Bibliography of U.S. Geological Survey water-resources reports for Utah, compiled by B. A. LaPray, U.S. Geological Survey, 1972. No. 23. Bibliography of U.S. Geological Survey water-resources reports for Utah, compiled by B. A. LaPray, U.S. Geological Survey, 1975. 69